ML20085M526
| ML20085M526 | |
| Person / Time | |
|---|---|
| Site: | Ginna  |
| Issue date: | 03/31/1977 |
| From: | ROCHESTER GAS & ELECTRIC CORP. |
| To: | |
| References | |
| RTR-NUREG-1437 AR, NUDOCS 9111110116 | |
| Download: ML20085M526 (78) | |
Text
O GINh A h UCLEAR POWER PLANT ROCHESTER GAS AND ELECTRIC CORPORATION O '
3161,a) DEMOh STRATION SUPP _EMENT NPDES PERMIT NO.070 OX2 2 000079 l (NY 0000493) l l
MARCH 1977 O
- aA22A8ue 77 1437 C PDR j A
.- . . _ _ _ . _ . _ _ _ _ . _ . ~ . _ . . _ . _ _ . . _ . - _ _ _ . _ . _ _ _ . _ . _ . _ _ . _ . _
h
-TABLE:OF CONTENTS GINNA 316 (a) DEMONSTRATION SUPPLEMENT-INTRODUCTION
SUMMARY
AND CONCLUSIONS
- 1. THERMAL PLUME CHARACTERISTICS 1.1 Plant Description 1.2 Heat Dissipation System Description 1.3 System. operation 1.4 Thermal Plume Model and Characteristics 1.5- Definition of Discharge Zone and Mixing Zone
- 2. REPRESENTATIVE IMPORTANT SPECIES DETERMI"ATIONS
- 3. DISTRIBUTION, AT3UNDANCES,_ AND_ YEARLY FLUCTUATIONS OF RIS
-3.1 Macroflora:- Cladophora O' 3.2 Macroinvertebrates: Gammarus 3.3 . Fish
.4.- TEMPERATURE TOLERANCE INFORMATION AND _.
AREAS OF EXCLUSION 4 . 11 Discharge Considerations 4.2 .Thermals' Effects Upon RIS
- 5. ASSESSMENT OF__ ADDITIONAL PLUME EFFECTS 5.1 Plume Entrainment 5.2 Fffects on-Migration of Fish 5.3 Fotential for-Gas Bubble Disease APPENDICES 2A 1
__.__.m._...-________ -_
I l
I"TRODUCTION i
! This document (Supplement) supplements the data l
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cf a'Secticn 316(a) application for the Ginna Nuclear Power Plant- ( Application No. 070 OX2 2 000079; :.'Y 0000493)- for a; ternate effluent limitations' pursuant t0 Section 316(a) of
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r w ._' _- d recuired by the draft Section 402 permit dated May 22, 1970 fcr the 3inna Nuclear Power Plant issued ty EFA'in accord-ance with proposed effluent limitations and standards of perf:r.r.ance for stean electric generating facilities I (?roposed 40 c?R Part 423, 39 Fed. Reg. 3293, March 14,
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I 1970). 'This-submissien was further supplenented on August 23,-1974 by a Demonstration Type ::: (protection of representative important species). These proposed regu-laticns required closed cycle cooling fer exircir.- ": vie plants of the Ginna'?c'.ter Flant size cat e-: :ry c r, alter-
- natively, an exemp:1cn autheriting -once-througn cooling g s er related-discharge limita:icns under criteria estat-
.:ned under See:1cn 316(a) of the FWP A. That Ginna 316(a)
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ru now pending in -the adjudicatory hearing proceedings for the t
Ginna Nuclear Power Station. It should be noted that this right is specifically recognized in stipulations to be signed in-settlenent of the Section LO2 pernit issues.
In the course cf conferences cc.tvened to resolve the thermal' issues raised in the adjudicatory hearing ,
i request, EPA requested additional information fron RG&E with regard to its 316(a) showing, since, subsequent to sub-mission of RG&E's-316(a) report en July 30,. 1974, as supple-nented en August- 23, 1974, EPA has publibbed additional information on the subj ect of 316(a) demonstration evidence. -
RG&E agreed to submit the requested additional inf:rnation in thf s Sd;;1enent ir acccrdance ,sith guideli. nee set forth in a letter dated Novenber 9, 1976-from Harvey Lunenfeld of EPA Region II to Roger W. Eober of RG&E. In addition to the specifications provided in.this'1etter, this Supplement .has been! prepared on the basis .cf agreement
- uetween ' RG&E and the EPA Staff with regard to the definition
..of the scope of informaticn to be provided in this Supple-mentlas weli as the appropriate f:rmat for its presentation.
= In some ' instances, R3&I has _ incorporated .b:, reference _ dis-cussions from its Section-316(a) and'Section-316(t, den:n-stration for the' Sterling Muclear-Power Plant. .This document is entitled "The Sterling Power Proj ect -
Vi
O
!:a:1 ear " nit !!o . 1, Volume 4 - Water Permits" and copies thereof have been provided to EPA, Region II. This proce-du e is used with the expressed approval of EPA.
Finallj, it is recctnized that there may be some inconsistency between thir Supplenent and the Section 316(a) d: ument submitted on July 30, 1970 Wherever this Supple-mert is inconsistent with the previous document, the state-
.er.ts ir thic Supplement shall supersede those in the 1974 d :: ur.e r t . Thic Supplener.: referer:es two additicnal years (1970 and 1975) of ecolcrical studies at the Ginna site and surr.2 rices effects cf Ginna operations upon the Representa-t i te Irr rrtant Species over the period 1969 to 1975. Data g
usei f-" verification of therm:1 plume modelling includes
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TABLE OP CONTENTS ggg CHAPTER 1: THERMAL PLUME CHARACTERISTICS Section Page 1.1 PLANT DESCRIPTION....................... . . . . . . . . . . 1.1 1.2 HEAT DISSIPATION SYSTEM DESCRIPTION ............... 1,1 1.3 SYSTEM OPERATION..................... .............s .1.?
1.3.1 Circulating Water System.................... 1.?
1.3.2 Recircu1ati n............................... 1,9 1.3.3 Biocide Treatment........................... 1.3 1.3.4 Reactor Shutdown............................ 1.3
.4 THERMAL PLUME MODEL AND CH ARACTERISTI CS . . . . . . . . . . . . . 1. 4-1 1.4.1 Mathematical Model Used..................... 1.4-1 1.4.1.1 Discussion of Model............ 1.4-1 1.4.1.1.1 Introduction................... 1.4-1 1.4.1.1.1.1 Problem Description............ 1.4-1 1.4.1.1.1.2 Poscible Tolution Methods...... 1.4-1 g 1.4.1.1.1.3 Other Empirical '!odels . . . . . . . . . 1. 4-2 W 1.4.1.1.2 Analytical Discussier.......... 1.4-5 1.4.1.1.2.1 Des cribing Paramete rs . . . . . . . . . . 1.4-5 1.4.1.1.2.2 Co.iterline Tempe ra ture Exces s . . 1. 4-6 1.4.1.1.2.3 Plume Half Width............... 1.4-12 1.4.1.1.2.4 Lateral Distribution........... 1.4-14 1.4.1.1.3 Data Description............... 1.4-16 1.s.l.1.3.1 Data Collection ............... 1.4-16 1.4.1.1.3.2 Data Rance..................... 1.4-16 1.4.1.1.3.3 Surface Data Reduction......... 1.4-17 1.4.1.1.3.4 Subsurf ace Data Reduction . . . . . . 1. 4-17 1.4.1.1.4 Statistical Methods and Resulting Equations............ 1.4-18 1.4.1.1.4.1 Statistica l Methods . . . . . . . . . . . . 1. 4-18 1.4.1.1.4.2 Centerline Temperature Excess.. 1.4-19 1.4.1.1.4.3 Plume Half-Width............... 1.4-22 1.4.1.1.4.4 Lateral Distribution........... 1.4-24 1.4.1.1.4.5 Possible Sources of Data Scatterl.4-25 1.4.1.1.5 Model Application.............. 1.4-26 1.4.1.1.5.1 Isotherm Construction.......... 1.4-26 1.4.1.1.5.2 Worst Case Isotherms.......... 1.4-26 1.4.1.2 Comparison of '!adel With Data...l.4-28 1-i
TABLE or CONTENTS Cl! APTER 1 (Continuud)
~
l Section Paae 1.4.2 Thermal Effects of Discharge................ 1.4-30 ,
1.4.2.1 Ambient Condition s . . . . . . . . . . . . . 1. 4- 30 1.4.2.2 Lake Bottom Temperature Rise... 1.4-30 :
1.4.2.3 Ve l oci t y De cay . . . . . . . . . . . . . . . . . 1. 4 - 31 ,
1.4.2.3.1 Exposure Time.................. 1.4-31 1.4.2.3.2 Plume Trajectory............... 1.4-32 1.4.2.4 Winter necirculation........... 1.4-33 1.4.2.5 seasonal Thermal Effects....... 1.4-35 1.4.2.5.1 Expected Seasonal Conditions... 1.4-35 1.4.2.$.1.1 Expected Winter Pluno.......... 1.4-35 1.4.2.5.1.2 Expected Spring Plume . . . . . . . . . . 1. 6 35 1.4.2.5.1.3 Expected Summer Plumo.......... 1.4-36 1.4.2.5.1.4 Expected rail Plume............ 1.4-36 i 1.4.2.5.2 Extreme Seasonal conditions.... 1.4-37 1.4.2.5.2.1 Extrerce Winter Plume........... 1.4-37 1.4.2.5.2.2 Extreme Spring Plume........... 1.4-37 t
1.4.2.5.2.3 Extreme Summer Plume............U.4-37 1.4.2.5.2.4 Extreme Pall Plumo............. 1.4-30 1.4.2.6 Parametric Plume-Analysis...... 1.4-30 m 1.4.3 Physical Effects of Discharge............... 1.4 41 U 1.4.3.1 Velocity Effects.............. 1.4-41 1.4.3.1.1 Surface Velocities............. 1.4-41 1.4.3.1.2- Bottom Velocities.............. 1.4-41 1.4.3.2 Concentrations................. 1.4-42 L 1.4.3.3 Shoreline Erosion.............. 1.4-43 References................................................ 1.4-44 s
1.5 LETINITION Or DISCHARGE ZONE AND MIXING ZONE........ 1.5-1 r
.- 1-11 f'
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m.nJ.,..,.. .Q._%.,_A.,_ .i.,.#._.. , . .._.._...._,._.,.,,,,,,__.,_,,_,..,,..._,,_.._.___,._,_.,_m.__.._.._...n... m
LIST OF TABLES Table !!o. Title J.4-1 List of Variables Used in Discussion of ".athematical "odel 1.4-2 Basic Parameters of Survevs Used to Develop 'dodel 1.4-3 Ginna Surface Isotherm Data 1,4-4 Ginna Six Foot Depth Isotherm Data 1.4-5 Correlation constants and Statistical nesults for the Ginna Data Tcpresentation 1.4-6 Ginna Lateral Distribution and Formalized Gaussian Distributien l.4-7 fionthly Difference in Ambient Temperature between the Shoreline and 5000 reet Offshore in the Ginna Vicinity as Given by C%ermack and Galletta (20) 1.4-8 Seasonal Discharge and Ambient conditions 1.4-9 Surface Centerline Excese velocity Decay for Seasonal Conditions 1s4-10 Ginna Triaxial Surveys 1.5-1 Ginna Discharge "ones 1.5-2 Ginna Mixing Zones 1.5-3 Ratios of Seasonal Thernel Plumes to the Ginna "ones of Impact O
l-lii 1
a
LIST OF TIGURES Fiaure !!o. Title
-1.4-1 Design Curves Describing the Ginna Thermal Discharge Plume 1.4-2 Comparison of Pessible Froude fiumber runctional Forms 1.4-3 Comparison of Hypothesized Relation Between T l and x with Values Determined at Ginna 1.4-4 Triaxial Survey Map 1.4-5 Range of Ginna Thornal Survey Densimetric Froude >
11umiers and Lake Elevations 1.4-6 Dimensionless Centerline Temperature Excess and Half Width Measured on 9/25/70 at the Lake Surface 1.4-7 Dimensionless Centerline Temperature Excess and Half Width Measured on 10/27/71 at the Lake Surface 1.4-8. Dimensionless Centerline Temperature Excess and Half Width Measured on S/1/70 at Six. Foot Depth )
1.4-9 Dimensionless Centerline Temperature Excess and Half Width Measured on 10/1/73 at Six Foot Depth ;
1.4-10 Dimensionless Centerline Temperature Excess-surface.
1.4-11 Dimensionless Centerline Temperature Excess-Six Foot Depth 1.4-12' Dimensionless Plume Half Width-Surface 1.4-13 Dimensionless Plume Half Width-Six Foot Depth-LO 1-iv
{
LIST Cr TIGURES (continued) rigure No. Title 1.4-14 Lateral Temperature Distribution 1.4-15 Variation of Densimetric Troude Mumber (T) Pith Lake Conditions for the Ginne Discharce 1.4-16 Linear Scale Factor vs. Lake Elevation 1.4-17 Dimensionless Centerline Temperature T.xcess and Half Width Measured on 9/11/75 at the Lake Surface 1.4-16 Dimensionless Centerline Temperature rxcess and Falf Midth Measured on 9/11/75 at six root Depth
> 1.4-19 Dimensionless Centerline Temperature Exceso and Half Width Measured on 10/21/75 at the Lake Surface 1.4-20 Dimensionless Centerline Temperature Excess and 9
Half Uidth Measured on 10/21/75 at Six root Depth 1.4-21 Dimensionless Centerline Torperature Excess and Half Width Measured on 5/24/76 at the Lake surface 1.4-22 Dimensionless Centerline Temperature Excess and Half Width Measured on 6/10/76 at the Lake Surface 1.4-23 Dimensionless Centerline Temperature Excess and Half Width Measured on 7/6/76 at the Lake Surface 1.4-24 Dimensionless Centerline Temperature Excess and Half Width Measured on 9/13/76 at the Lake Surface 1.4-25 Dimensionless Centerline Temperature Execrs and Half Uldth Measured on 9/29/76 at the Lake Surface 1.4-26 Dimensionless Centerline Temperature Excess and Half Midth Measured on 11/5/76 at the Lake Surface 1-v
-(]) LIST OF FIGURES (continued)
Floure Mo. Title }
1.4-46 Expected and Extreme Seasonal Isotherm Volumes .
1.4-47 Time - Temperatura Decav, Expected Spring conditions 1,4-48 Time - Temperature 9ecay, Expected Summer conditions 1.4-49 Time - Temperateer L.7ay, "'poeted Pall conditions !
1.4-50 Time - Temperats te 52cey , Extrone Spring Conditionn '
1.4-51 Time - Tempersture Der;ay, Extreme Summer r>>nditions 1.4-52 Time - Temperature Decay, Extreme Fall Conditionc
-1.4-53 Expected Spring Plume Trajectories 1.4-54 Expected Summer Plume Trajectories 1.4-55 Expected Fall Plume Trajectories 1.4-56 Extreme Spring Plume Trajectories 1.4-57 Extreme Summer Plume Trajectories 1.4-58 Extreme rail Plume Trajectories 1,4-59 Expected 2'F Surface Isotherm Areas 1.4-60 Expected 2'T Surface Isotherm Areas 1.4 Expected 5'F Surface Isotherm Areas 1,4-62 Expected 10'F Surface Isothern Arees -
1.4-63 Expected 2'F Six Foot Depth Isotherm Areas 1.4-64 Expected 3'F Six Foot Depth Isotherm Areas 1.4-65 Expected 5'r Six Foot Depth Isotherm Areas
'1.4-66 -Expected 10'T Six Foot-Depth Isotherm Areas O 1-vi
_ _ . - - . . _ _ . _ _ _ _ . _ . _ , _ . . . _ _ _ _ . _ . _ _ _ _ _ _ . _ . _ . _ _ _ _ _ _ ...__s___.,__._..-,_._..
LIST Or TIGURES (continued) rigure No. Title 1.4-27 Discharge Velocity vs. Lake Elevation 1.4-28 Discharge Flow Eates During Recirculation 'tode 1,4-29 Lane Furface Isotherms - Fxpected Fprinc ccnditier.c 1.4-30 Six root Depth Isotheres - Expected Sprino Conditions 1.4-31 ?ake Surface Isotheres - Expected Summer Conditions 1.4-32 Six Foot Depth Isotheres - Expected Summer Conditions 1.4-33 Lake Surface Isotherms - Expected rail Conditions 1.4-34 Six root Depth Isotherms -
Txpected rall Conditions 1.4-35 Lake Surface Isotherms - Extreme Spring Conditions 1.4-36 Six root Depth Isotherms - Extreme Spring Conditions 1.4-37 Lake Surface Isotherms - Extreme Summer Conditions lll 1.4-38 Six root Depth Isotherms - Extreme Summer Conditions 1.4-39 Lake Surface Isotheres - Extreme rall Conditions 1.4-40 Six root Depth Isotherrs - rxtreme rail Conditions 1,4-41 Isotherm 1.rees along Lake Surface - Expected Seasonal Conditions 1.4-42 Isotherm Areas at Six root Depth - Expected Seasonal Conditions 1.4-43 Isotherm Areas clerg Lake Surface - Extreme Seasonal Conditions 1,4-44 Isotherm Ireas at Six root Depth - Extreme Seasonal Conditions 1.4-45 Isothermal Lake Bottom treas Expected and Extreme Seasonal Conditions k 1-vii
i (f LIST OF FIGURES (continued)
Figure '!o. Title ,
1.4-67 Average and tiaximum Isothermal Lake Bottom l Areas - Ta
- 40*I 1.4-6B Average ac !!aximum Isothermal Lake Bottom ;
Areas - T a = 60'F i
1.4-69 Average and Maximum Isothermal Lake Dottom ;
Areas - Ta = 80'F i 1.4-70 Worst Case 2'T Surface Isotherm Areas _
1.4-71 Worst Case 3'T Surface Isotherm Areas 1.4-72 Worst case 5'T Surface Isotherm Areas 1.4-73 Worst Case 10'T Surface Isotherm Areas 1.4-74 Worst Case 2*F Six Foot Depth Isotherm Areas 1.4-75 Worst Case 3'T Six Foot Depth Isotherm Areas 1.4-76 Worst Case 5'T Six Foot Depth Isotherm Areas 1.4-77 Worst Case 10'r Six Foot Depth Isotherm Areas 1.4-78 Time - Temperature Decay, E a 244 Ft. USGS 1.4-79 Time - Temperature Decay, E = 246 Ft. USGS _;
1.4-80 Time - Temperature Decay, E = 248 Ft. USGS 1.4-81 Time - Temperature Decay, E = 250 Ft. USGS 1.4-82 Average and !!aximum Lake -Bottom Scour Areas i (Bottom Velocity >1' FPS)-
1 1- viii ,
- n. .
LIST OT TIGURES (continued) ggg rigure No. Title 1.5-1 3'r Discharge "one Development - Lake surface 1.5-2 3'r Mixing "one Developrent - Lake Surface 1.5-3 Isothernal Discharge ".ones - Lake Surface 1.5-4 Isothermal Discharge Zones - Six Foot Depth 1.5-5 Isothermal Discharge Zones - Lake Botton 1.5-6 Isothernal Mixing "ones - Lake surface 1.5-7 Isothernal Mixing Zones - Six Foot Depth 1.5-8 3'r Lake Surface Impact "ones with Expected 3'T Spring Isotherm 1.5-9 3'r Six Foot Depth Impact Zones with Expected 3'r Spring Isctherm lll 1-ix 9
t O
SUlFARY AND CONCLUSIONS Ginna Nattent Pcwei Plant .
316(a) Devonslution Supplement The following statements are summaries and conclusions of the data and material contained in this document. Section numbers, which present complete discussions of the bases or reasons for each state-ment, are included in parenthesis.
- 1. The water cuality related discharges from the Ginna Plant are governed by a final National Pollutant Discharge Elimination System (NPDES) permit issued for this facility in February, 1975. The Ginna Plant discharges are in compliance with all
-chemical limitations specified in that permit. The purpose of this report is to provide supplemental information necessary for the determination of the therral limitations for the existing ,
discharge. (Introduction)
() 2. The Ginna Nuclear Powee Plant is licensed to at power levels up to 1520 MWt. A pressurized-water ermit operations reactor (P'fR) is used to produce thermal energy. A steam turbine-generator uses this heat to provide 490 MWe (net) .of electri- '
cal power output. (1.1)
- 3. Heat-removal facilities for normal operation consists of a con-ventional once-through system with cooling water being withdrawn from and returned to Lake Ontario. The total circulating water flow of 400,000 GPM is withdrawn through a submerged octagonal intake structure that lies some 3100 f t off shore in about 35 f t of water and is returned to the lake via a canal as a shoreline surface discharge. Retention time of condenser coo 33ng water in the plant system is about eight minutes. (1.2)
- 4. The waste heat released-to Lake Ontario hy the plant is about
- 4. 0 x 109 BTU /HR at 490 MWe of rated output. The 400,000 GPM flow is ncrmally maintained at all power levels. A temperature r increase of 20P' has been assumed across the condenser cooling
-and service water systems for calculationsaof waste heat rejec-tion, (1.3.1)
- 5. A dimensionless empirical model of a heated surface discharge into shallow water was derived. Five years of thermal survey data at the Ginna site were used to determine the model con-
- A stants. Both surface and six foot depth thermal distributions
- were simulated. (1.4.1.1) viii
O
- 6. The model was compared with both the five years of thermal survey data used to determine the model constants plus eight independent surveys not used in the model development. Good agreement was found. (1.4.1.2)
- 7. Bottom temperatures (1.4.2.2) and velocities (1.4.3.1.2), based on field measurements, were also simulated. 3'T bottom contact occurs within approximately 1000 feet of shore (1.4.2.2). Lake botton scour areas are less than 5 acres (1.4.3.1.2).
B. Seasonal expected and extreme ambient conditions were found (1.4.2.1). The thermal effects of the Ginna discharge during each seasonal condition were simulated. The largest thermnl effects, exclusive of winter conditions, were generally found in the spring (1. 4 . 2. 5 ) . The expected 3'r sprino isotherm has creas 6n the lake surface, 6 foot depth, and bottom of 86, 32, and 5.6 acres, respectively. (1.4.3.5.1.2)
- 9. Winter effects, although not explicitly modelled were estimated based on mechanistic considerations (1.4.2.4). The winter plume was f ound to be of the same general size as the other seasonal plumes (1.4.2.5.1.1, 1, 4. 2 . 5 . 2.1) .
- 10. Segmental impact zones to the 3'r isotherm are utilized as a ba"is &
W for the areal assessment of any thermal impacts upon the acuatic ecosystem. ones of impact are classified as a DISCHARGE CONE and and MIXING ZONE. The DISCHARGE "ONE is evaluated cuantitatively due to the high frequency of plume occurrence. The "IF!rG CCNE is addressed on a qualitative basis due to its low probability of occurrence. The area of the DISCHARGE ZONE at the surface, C foot depth, and bottom is 176, 65 and 11 acres, respectively. The zones of impact defined herein conservatively exceed the areal dimensions of the e::pected and extreme therral plumes of the Ginna discharge.
(1.5)
- 11. Representative Important Species (RIS) designated for the acuatic ecosystem at the Ginna site are Cladophora, Gammarus, Alewife, Smelt, Spottail Shiner, Smallmouth Bass, White Perch, Coho Salmon and Brown Trout. Rationale for selection of these species is pro-vided in discussions contained in the Sterling 316(a) Demonstration and incorporated herein by reference (2.0).
- 12. The macroflora community at Ginna Station is composed entirely of Cladophora olomerata, the abundance of which decresses lakeward and is essentially absent by six meters of water depth. Claderhora demonstrates random yearly abundances, with the variance amona years at eacn transect greater than the variance amono transects for each year. A lastina effect of the discharge cannot be detected (3.1).
O ix
t
()
l
- 13. The macroinvertebrate community, represented by Gammarus, shows '
- typically greater _ concentrations at the two and five meter depths, diminishina lakeward from the five meter depth. No significant differences in abundance have been found between the transects even thouch the distribution of Gammarus appears to be patchy. Annually, abundances of Gammarus are relatively stable. The discharge does not
seem te have an adverse impact on this community (3.2).
- 14. The fish not studies conducted at the Ginna site from 1969 through 1975 have supplied information upon which the RIS fish have been '
chosen. These species, listed in order of decreasing Catch per ,
Unit Effort (CUE), are: Alewife, White Pcrch, Spotta11 Shiner, Rainbow Smelt, Smallmouth Bass, Brown Trout and Coho Salmon.
Each RIS fish population et the Ginna Site has been analyzed with :
t respect to general distribution and abundance, relationship to the thermal plume cased on perference temperatures and swimming abilities, attraction to or avoidance of the plume based on collected data, use of the site as a spawning or nursery area, and yearly fluctuations in abundance. A final section deals with all of the above areas on a-total RIS-fish community basis. (3.3)
( ) 15. Seasonal preference temperatures and swimming capabilities for each RIS fish are discussed relative to acclimation temperature and other modifying factors. These data are variously utill:cd in other sections to both predict and verify actual responses of fish to the Ginna discharge, and to determine their potential for plume penetration-and possible impact (3.3.3.2, 3.3.4.2,
- 3. 3. 5.2, 3.3.6.2, 3.3.7.2. 3.3.6.2.3.3.9.2).
- 16. RIS fish show varying degrees of attraction to and avoidance of the thermal p]ume during the course of thu year based upon an Attraction Index. All species appear to behave generally in good agreement with their-thermal preferenda and migratorv instincts. This results in apparently minor effects upon the_RIS fish community, in that these species fluctuate seasonally, showing that natural behavior patterns are dominant over influences of the thermal plume (3.3.10.2).
- 17. Fish egg and larvae studies have identified the following RIS-fish larvae at the Ginna sites alewife, smelt, white perch and shiners.
Utili:ation of the site as a spawning or nursery area is assumed to be predominated by alewives, while other species may use it spora-- -'
dically. Some species (coho salmon and brown trout) are not assumed to be able to naturally reproduce in Lake Ontario or its tributaries.
l Spawning intensity seems normal for each RIS in accordance with their i -species-specific habitat recuirements. The area does not appear
() to be a preferred or unique spawning er nursery area for any RIS-fis'r . i 3. 3) x
- 18. A quantitative assessment of theoretical thermal impact, expressed in terns of tire and areas within the discharge zone frcm which organisms might be excluded, is provided for each RIS. Exclusion areas occur either at the surface, six-foot depth, or region of g
plume bottom-contact, depending upon the behavior and habitat of each species they represent portions of the discharge :cne where upper thermal tolerances are exceeded for varicus life activities such as parent survival, sumscr survival, growth (optimal and acceptable), reproduction, and development (4.1, 4.2).
Species - specific conclusions derived from this theoretical approach are as follows:
Macroflora (Cladophora, - Considering the extremely small areas of bottom contact (less than six acres) and time in surner when parent stock may be excluded, and considering the absence of potential thermal impact on all remaining life activities outside from the scour zone, it is reasonable to expect the Ginna plume to have a negligible adverse impact on Cladophora (4.2.1).
Macroinvertebrates (Gammarus) - Given the absence of potential thermal impact on survival of adult gammarids, the extremely small areas of plume bottom - contact and brief periods of impact on eggs, immatures, and reproduction, and lastly the predicted suboptimal growth within a small area during summer ,
it appears unlikely that the Ginna discharge could have a significant, much less a measureable, adverse thermal impact on Gammarus , hence the macroinvertebrate connunity (4. 2. 2) . llk Fish (Alewife)-- To summarize potential thermal effects of the Ginna discharge upon alewives, the applicant anticipates a small area of possible exclusion for nature fish in July, very small areas consistently or larger areas for brief tire periods excluding juveniles in summer, suboptimal growth in various portions of the discharge zone mostly in summer (assuming alewives remain there for weeks or months), and finally negligible thermal impact on their development and reproduction activities. On this basis the applicant concludes no appreciable adverse thermal impact on the alewife population (4.2.3.1).
(Smelt) - Due to smelt's preference for cold water, and its normal distribution in deepf offshore waters in the summer, the potential for thermal impact on this species is expected to be minimal. Reproduction and development activities would not be thermally impacted apart from the maximum scour zone (4.2.3.2).
(Spottail Shiner) - The applicant anticipates no consequential thermal effects on either reproduction, development, or parent survival of spottail shiners within the Ginna discharge zone.
The potential for direct impact on spottails, and suboptimal grewth within various sized areas in surrer, is minimized by 3 W
their general avoidance of the nearshore area at this time
(,.:.3.3).
xi
(Whito Perch) - The applicant finds no potential thermal :
impact on reproduction, development, and parent survival with- >
in the Ginna discharge zone.
() exclusion of white perch from small areas during the warmest part of summer, and a potential for suboptimal growth in areas There is a potential for some of various dimensions during the summer months. Enhancement of food reserves in and about the discharge may compensate for thermally induced suboptimal growth, and serve to minimize the extent of potential impact (4.2.3.4),
(Smallmouth Dass) -
To summarize the findings of a theoretical thermal impact asses.mont on various life activities of small-mouth bass, one could safely conclude that the Ginna discharge has a negligible impact on development, reproduction, and parent survival, and would exclude individuals from inhabiting
- very small areas (less than 3.5 percent of the discharge zone) during the summer. Growth could be suboptimal within reason-ably small subsurface areas, however enhanced availability of food resources may compensate for such potential effects (4.2.3.5).
(Coho Salmon) - The applicant's evaluation of theoretical thermal impact on echo salmon of Lake Ontario, has demonstrated a low potential for impact on mature forms migrating through the region beneath the discharge zone in late summer and October, and a minimum potential impact on acceptabic growth of individuals occupying the discharge zone in spring and fall (4.2.3.6).
) (Brown Trout) - The results of a theoretical impact assessment on brown trout at Ginna suggest no impact on mature specimens occupying nearshore waters in the fall, though there is a possible exclusion from a small area of the discharge zone should sone individuals migrate shoreward earlier (September) .
The potential for impact on growth (optimal and acceptable) should be greatly minimized in summer since brown trout occupy waters somewhat offshore within their preferred temperature range. No significant impact is predicted on growth in late spring. Successful reproduction and development of this stocked species is questionable in Lake Ontario; there-fore the applicant anticipates no potential for thermal im-pact on these activities (4.2.3.7).
- 19. A species-specific evaluation of cold-shock ef fects, stemming from a reactor shutdown (rapid or scheduled), indicates a potential l for low impact and a confinement of possible effects to specific colder months. Minimal concentrations of rainbow smelt, coho L salmon, and brown trout might experience cold-shock during winters l spottail shiners and white perch could b3 stressed and/or cold-shocked only in February; alewives are prone to impact mainly in April; and smallmouth bass are never expected to experience cold-shock.
In. general, the extent of potential impact would be slight based on the few individuals inhabiting discharge waters during cold months,
(~' and is not expected to adversely affect protection and propagation of RIS fish at Ginna (4.2.3.1-7).
xii l
= r. - - - - my'- - .,- . _ . ,
e- ~ --gr .y 7.i,--- ,+.---g_, e 9-r----m,_-,.--wwy,--,.,__,.
- 20. The plume entrains local lake water and transports it out into the lake. This offshore transport of lake water is replaced by an ecual onshore movement of water. Such a countercurrent is usually found beneath the plume and has its origins of f shore of the plume area.
g The flow rate of water entrained into the plume was calculated as a function of temperature and plume location. The maximum flow of entraining water exposed to 3*T temperatures or higher with expected spring conditions is approximately 2700 cfs (5.1.1).
- 21. Munbers of organisms which may be entrained into the plume have been cetimated based upon (1) the concentrations of fish eggs and larvae and the RIS-Gammarus found at the Ginna site, and (2) calculations of the volume of water entrained. These esti-mates are presented for the period of May through September which would be the period of highest concertrations for such organisms.
Considerations and findings of this plume entrainment assessment includes (1) evidence of a linnetic countercurrent which flows shoreward beneath the thermal plume which may significantly reduce entrained organisms, (2) an incionificant thermal stress imposed upon Gammarus and a slicht displacement of some of these organisms, (3) miner entrainment of fish eags since most found near the Ginna site are dimersal, and (4) indications that larvae entrained into the plume would not reach detrimental temperatures. Overall, en-trainment into the thermal plume has not be determined to result in adverse impact upon the RIS (5.1.2).
- 22. Fish tagging studies conducted from 1973 through 1976 support evidence that little, if any, interference to fish movements along llh shore may be attributed to the Ginna thermal discharge into Lake Ontario (5.2).
- 23. Gas bubble disease (GBD), a condition which may develop in fish subjected for a critical species-specific period of time to dis-charge waters supersaturated with a critical concentration of total gases and/or threshold ratio of dissolved oxygen to nitrogen, has neither been, nor is expected to be, a problem at the Ginna discharge. Support for this conclusion is derived from studies on L. Michigan where it was demonstrated that sensitive species such as brown trout, coho salmon, spottail shiners and others, captured from supersaturated discharge waters, did not exhibit symptoms of GBD. The author attributes these findings to short residence times of fish in critical areas of potential impact.
This behavior, coupled with a paucity of fish observed occupying discharge waters at Ginna during critical periods (mainly winter months), greatly minimizes potential impact. Actual observed
. occurrences of GBD at the Ginna site have been rare (5.3).
This suppicment dcronstAatc5 hat the shorelinc su%facc dischauc cl the Ginna j Mactcat Pcwc1 Plant assures the pretcetion and ptenapation e! a balanced in-1 diacncut aouatic comunibt as excnlified by the Reptesentative impcttant
~
Scccic: at 'the Ginna Sitc'. &
xiii l
O CHAPTER 1.0 THrR'ML PLtNr CHAPACTERTSTICS 1.1 PLM?T DESCRIPTION The Ginna Nuclear Power Plant is located on Lake Ontario in the northwest corner of Wayne County, N.Y. This location, on the south shorn of Lake Ontario, is about 20 miles ENE of Rochester, N.Y. and 45 miles WSW of Oswego, N.Y. Figure 1.1-1 shows the ccunties and the larger cities and towns within 50 miles of the site. The nearest planned and exis-ting nuclear facilities are located at the Sterling site (about 34 miles away) and Mine Mile Point Units (about 49 miles away), respectively.
Rochester Gas and Electric Corporation (RG&E) obtained its provisional license on September 19, 1969 to operate Ginna at 1300 uegawatts thermal (MWt) . The AEC Directorate of Licensing amended this provisional operating license to RG&E on March 1, 1972 to allow operation at power 3evels up to 1520 MWt. A preasurized-water reactor (PWR) is used to pro-duce this tAermal power level. A steam turbine-generator uses this heat to provide 490 MWo (not) of electrical power capacity.
llh The plant consists of a closed-evele, pressurized, light-water-moderated nuclear steam-supply system, a turbine-cendenser system, and auxiliary equipment. Figure 1.1-2 is a simplified flow diagram of the steam-electric svstem.
After passing through the turbines, spent steam is condensed by once-through cooling with water from Lake Ontario. At full design power, the plant removes water trom Lake Ontario at the rate of 400,000 GPM and heats it to a temperature 20P' above ambient lake temperature before returning it to the lake as a shoreline surface discharge.
1.2 HEAT DISSIPATION SYSTEM DESCRIPTION Heat-removal facilities for normal operations consie';w of a conventional once-through system with cooling water being withcrawn from and returned to the same waterlody. The intake-discharge f acilities are designed to provide the water recuirements for the circulating water system and the house service water system. The total flow of circulating water through these systems under normal operating conditions is about 400,000 GPM (891.2 CPS). Figure 1.2-1 is a flow dia-gram of these once-through systems. Lake Ontario is the O
1.1
i
() source and recipient of the circulating water which is withdrawn through a submerged octagonal intake structure that lies some 3100 ft offshore in about 35 ft of water.
Figure 1,2-2 is a perspective drawing of the intake struc-ture, screenhouse and discharge canal. Intake water flows by gravity through a 10 ft diameter concrete-lined tunnel into the screenhouse, where it p6sses through a coarse screen and fine-mesh traveling screens before being pumped to the condenser or service water system. The water from these two systems is combined and released to the dischargc canal which opens into Lake Ontario at the shoreline. The discharge canal is an open structure approximately 20 ft wide at the base with side slopes of 1:1 at lake entry.
Average water depth in the canal is about 8 ft and a dis-charge velocity of 3.7 fps is typical. The 400,000 GPM flow is normally maintained at all power levels and its discharge velocity, which depends upon en lake elevation, is presented in Figure 1.4-27.
1.3 SYSTE'1 OPERATIOD 1.3.1 Circulating Water System The waste heat released to Lake Ontario by the plant is about 4. 0 x 109 BTU /HR at the 490 MWe rated output. The water used to remove heat from the main condensers is pro-(]) vided by a once-through circulating svstem designed to limit the temperature rice thrcugh the main ecndensers to a naximum of approximately 20F* at 100 percent of rated ca-pacity. As presented in Figure 1.2-1, 381,000 GPM of the measured 400,000 GPM total circulating water flow passes through the condensers and 19,000 GPM flow through the ser-Vice water system. A temperature increase of 20F* has been assumed across the service water system for calculations of waste heat rejection.
The 400,000 GPM circulating flow is normally maintained at all power levels except during periods of recirculation to prevent the accumulation of fra:11 ice on the intake struc-tures. Retention time of condenser cooling water in the plant system is approximately eight minutes and no consump-tion or process contact of the water occurs.
1.3.2 Recirculation During normal operating conditions, at rated thermal power, the temperature of the water that leaves the discharge canal is increased about 20T* above the temperature of withdrawal from Lake Ontario. During the period from mid-December through mid-April, a portion of the condenser discharge water O
1.2
O is recirculated to the forebay to prevent any ice accumula-tion on the screenhouse facilities. Ginna operating pro-cedures state that condenser water inlet temperature should be maintained at no more than 40'r maximum by use of the re-circulation gate during the winter months. Discharge flow rates versuo temperature excess during the recirculation mode are presented in Figure 1.4-28. Under such conditions of maxinum recirculation, the temperature of the discharge water to Lake Ontaric would be increased 28P' above inlet water tem-peratures. Recirculation has the effect of lowering tha flow rate while raising the discharge excess temperature.
Plume development with reference to winter recirculation is discussed in section 1.4.2.4.
1.3.3 Biocide Treatment Sodium hypochlorite is intermittently added to the intake water at the forebay to inhibit biological growths and main-tain heat transfer efficiency in the main condenser and house service water systems. Total residual chlorine is con-tinuously monitored during chlorination periods.
- n January 1977, chlorination procedures at Ginna have been reduced to one 30 minute period per day five times por week inanefforttokeepchlorinedischarceserlowaspracticablejlh The facility is operating in compliance with its NPDES ef-21.xte
- imitation of 0.5 ng/l free available chlorine and ma xi: . value of 45.4 kg/ day (100 lbs/ day).
1.3.4 Reactor Shutdown Scheduled shutdowns for refueling and maintenance generally eccur once a year for about a six week period. It is ex-pected that the refue]ing outage would normally occur during the Spring or Fall when electrical system demands are at a minimum and not during the period December through March, except as recuired by New York Power Pool Planning (NYPP).
Cecrdination of planned shutdowns with NYPP is required so that an acceptable state power reserve is maintained.
Any changes in reactor power during operation will cause time-varying temperature behavior in the thermal plume. A normal startup or shutdown would typically result it. finer incremental temperature changes in the circulating water discharge than an emergency shutdown. The severest impact would result from l the simultaneous occurrence of the following conditions:
(1) full-power operation in winter, (2) maximum recirculation, (3) instantaneous decrease from full-power operation to zero-power, and
'4) continued operation of the main circulating water pumps.
g.
1.3
s l
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i
- The temperature drop of the discharge water associated with
! rapid outage would be most severo during the first minute i (about 17'F) . The average number of unscheduled shutdowms per year for the Ginna unit is 10 based upon a 5 year opera-tion period.
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O LIST OF FIGURES (continued)
Title Ficure "o._
1.4-67 Averace and Maximum Isothermal Lake Botto Areas - T3 = 40*F Average and Maximum Isothermal Lake Bottom 1.4-68 Areas - Ta = 60*F Average and Maximun Isothermal Lake Bottom 1.4-69 Areas - Ta = 80*F Worst Case 2*F Surface Isotherm Areas 1.4-70 Worst Case 3*F Surface %setherm Areas 1.4-71 Worst Case 5*F Surface Isotherm Areas 1.4-72 1.4-72 Worst Case 10*Y Surface Isotherm Areas Worst Case 2*F Six Foot Depth Isotherm Areas 1.4-74 3*F Six Foot Depth Isotherm Areas Worst Case s 1.4~75 Worst Case 5*F Six Foot Depth Isotherm Area 1.4-76 Areas Worst Case 10*F Six Foot Depth Isothern 1.4-77 244 Ft. USGS Time - Temperature Decay, E a 1.4-78 USGS Time - Temperature Decay , E = 246 Ft.
1.4-79 USGS Time - Temperature Decay, E = 248 Ft.
GS 1.4-80 Time - Temperature Decay, E = 250 Ft. US 1.4-81 Average and Maximum Lake Bottom Scour Areas 1.4-82 (Bottom Velocity >l FPS)
O l- viii T
f i
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{
(continued) i LIST OF TIGURES ,
-l rioure No.
Title Surface 3*r Dischen;, Mac Development - Lake ;
1.5-1 Develegent - Lake Eurface 3'T 1% v1 Ur.foi.* f ce 1.5-2 Isotheru! m eharge tones - Laket Depth Sur a 1.5-3 Isothevuof.1%scharge Zones - Six Foo 3 1.5-4 Isothy r#al Dischargo Zonas -f Lake Bottom '
1.5-5 Isothermal !!1xing tones - Lake Depth sur ace 1.5-6 Isotherrnal- itixing Zones - Six Foot td 1.5-7 3*r Lake Surface Impact Zones with Expec e 1.5-8 -l 3*r Sprin5J' Isotherm with Expected O- 3*r six root Depth I.mpact Zones r 1.5-9 3'F Spring Isotherm 1
i y
a 20 ix
c--- - ._ ___
i O
I CHAPTER 1.0 S
THrn'MLJyr CHt PAcTreIF"7C !
1,1 PLM:7 DESCRIPTION is located on This Lake Ontario location, in The Ginna Nuclear Power Planteio, County, is aboutN.Y,20 miles ENEFigure the northwest corner of Wayn on the south shore of Lake OntarWSW of Oswego, and towns N.Y.
of Rochester, N.Y. and 45 milescounties and the larger citiespl The nearest 1.1-1 shows the of the site. re located at the Sterling site49 (about within 50 miles tina nuclear facilities aand Nine Mile point Units 34 miles away)
(about respectively. obtained its miles away), tion (RG&E) Ginna 19, 1969 to operate of Rochester Gas andonElectric September Corpora The AEC Directorate provisional license thermal (MWt) 1300 megawatts i al operating
. license to RG&E Licensing amended this provis ontion at
) at power levels u on March 1, 1972 to allow operaA A steam pressurized-water turbine-generatorof ele rea 152C MWt.
duce this thermal power icvel.0 MWe (net) uses this heat to provide 49 capacity. d evele, pressurized, light-The plant consists of a close - upply system, a turbine-Figure 1.1-quipment. d water-moderated nuclear f the steam-scondenser steam-electric bines, spent steam is condense svstem.
At is a simplified flow diagram o After passing through the tur r f romto Lake Ontario. wa a temperaturo by once-through cooling d heats with it watefull desig it to at the rate of 400,000 GPM anlake temperature before retu 20P' above ambientshoreline surface discharge.
the lake as a TION 1.2 HEAT DISSIPATION lSYSTEM operationsDESCRIP consists of stem The Heat-removal facilities a conventional once-through d to for sythe norma same waterbody.
designed to provide the water withdrawn intake-dischargefrom and returne facilities areing water system and the house r s is water system. under normal operating co requirements for the circulat service 1,2-1 is a flow dia-FigureLakeOntarioisthegg through these systems ( 8 91. 2 CT S) .
400,000 GPM stems.
about gram of these once-through sy 1.1
O source and recipient of the circulating water which is withdrawn through a submerged octagonal intake structure that lies some 3100 f t of f shore in about 35 f t of water.
Figure 1.2-2 is a perspective drawing ofIntake the intake waterstrue-flows ture, screenhouse and discharge canal.
by gravity through a 10 f t diameter concrete-lined tunnel into the screenhouse, where it passes through a coarse screen and fine-mesh traveling screens before being pumped to the condenser or service water systen. The water from these two systems is combined and released to the discharge canal which opens into Lake Ontario at the shoreline. The discharge canal is an open structure approximately 20 f t lake entry.
wide at the base with side slopes of 1:1 at8 ft and a. dis-Average water depth in the caral is about
. charge telocity of 3.7 fps is typical. The 400,000 GPM flow is normally maintained at all power levels and its discharge velocity, which depends upon en lake elevation, is presented in Figure 1.4-27, 1.3 SYSm! OPEPATION 1.3.1 Circulating Water System
( )' The waste heat eleased BTU /HR to Lake Ontario by the. plant is at the 490 MWe rated output. The about 4. 0 x 10 water.used to remove heat fron the main condensers is pro-vided by a once-through circulating evste.m designed to limit the temperature rise through the main condensors to a naximum of approximately 20F' at 100 percent of rated co-pacity. As presented-in rigure 1,2-1, 381,000 GPM of the measured 400,000 GPM total circulating water flow passes through the condensers and 19,000 GPM flow through the ser-vice water system. A temperature increase of 20F* has been assumed 4 cross the service water system for calculations of waste heat rejection.
The 400,000 GPM circulating flow is normally maintained at all power levels except during periods of recirculation to ,
prevent the accumulation of frazil ice on the intake struc-I tures. . Retention time of -condenner cooling water in the plant system is approximately_eight minutes and no consump-tion or process contact of the water occurs.
1.3.2 Recirculation During normal operating conditions, at rated thermal power, the temperature of the water that leaves the discharge canal is increased about 20F' above the temperature of withdrawal from Lake Ontario. During the period from mid-December-O through mid-April, a portion of the condenser discharge water 1.2
.;.--_-.. . - . - - . _ - - . - . = - . - - - . - - - .- - .-- w. _
O ice accumula-
. is recirculated to the forebay to prevent anyGinna temperature operating pro should tion on the screenhouse facilities. by use of the re-cedures state that condenserhwater inlet flow Discharge be maintained at no more than h 40'r maximum rec circulation gate during the winter mont s. rates h discharge water are presented in Figure 1.4-28.
maximum recirculation, the temperature of t e8F'h above inlet to Lake Ontario would be increased 2temperature. Recirculation has peratures.
flow rate while raising the discharge excess circulation is Pluma development with reference to winter re discussed in section 1.4.2.4.
1.3.3 Biocide Treatment d d to the intake water at the forobay toh inhibit biolog main condenser andcSodium tain heat transfer ef ficiency in t eTotal residual periods. chlorine is con-i house service water systems.tinuously monitored during t Ginna have been W g
In Omnuary 1977, chlorination procedurer low afiveastimes per week practicable.
reduced to one 30 minute period per day in an effort to keep chlorine discharcos atith its NPDES ef-The facility is operating in compliance w l hlorine and fluent limitation of 0.5 ng/l free availab/ day). e c maximum value of 45.4 kg/ day (100 lbs 1.3.4 Reactor Shutdown i tenance generally It is ex-Scheduled shutdowns for refueling kdand period.
ma n normally occur during occur once a year for about b r athrough six weepected March, the Spring or Fall when electrica l ing (NYPP).
minimum except and not during the period Decem eas r is maintained.
Coordination of planned shutdowns witthat a tion will cause time-l plume. A normal Any changes in reactor ltpower during in finer incremental startup or shutdown would typically resuimpact from would o
temperature changes in the hcirculatThe severestfollowin an emergency shutdown.the simultaneous occurrence of winter, (1) full-power operation in tion to lll (2)
(3) maximum recirculation, instantaneous i g decrease from water pumps.
l (4) zero-power, andcontinued operation of the main circu at 1.3
~~~ _.
I t
O water associated with The temperature drop of the severe during the first minute discharge d tms rapid outage would Thebeaverage most nu~her of unscheduled shut obased upon (about 17'T).
per year for the Sinna unit is 10 ti.on period.
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Figure 1.1-1
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SIMPLIPIED FLOW DIAGRAM OF T!!E STEAM-ELECTRIC SYSTEM Or THE GINNA NUCLEAR POWER PLANT
-y lfgyg.......m.......<....;i . .
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LMUTDO*N COOLING NL At ( ACHANGI4 f>0W
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,I teNnfNsrN 3.i eco .r SI.':PL TIED FLOW DI AGIUdi OF Tilr CC" DENSER AND SERVICE-WA"ET SYSTD:S OF Tile GINNA MUCLE.' E POWTR PLANT .
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1.4 THEPPAL PLITE MODEL AND CHARACTERISTICS 1.4.1 MATHEMATICAL MODEL USED 1.4.1.1 Discussion of Model 1.4.1.1.1 Introduction 1.4.1.1.1.1 Problem Description When a stream of warm water is released from an open channel into a large body of water, the warmer effluent mixes with the cooler anbient water, resulting in spreading and cooling of tne discharge. The area in the receiving Lcdy where the discharge can be sensed is referred to as the thermal plume. The plume can be thought of as being comprised of four basic regions: the core region, in which the initial jet effect of the discharge results in a mixing of the plume with the ambient water but in which the temperature and velocity of the plume centerline remain essentially constant; the entrainment region, in which the turbulent shear forces caused by the velocity difference between the plume and ambient result in the mixing of cooler water with the discharge plume while the buoyancy of the warmer water tends to cause the plume to rise; the stable region, in gg) which the plume continues to spread due t; the buoyant rising of the warm water but in which the rate of entrainment is inhibited by the low plume velocity and the high density stratification between the plume and ambient; and the far field, in which the plume surface area is large enough to allow significant heat transfer from the lake to the atmosphere.
This discussion is intended to concentrate on the near field por-tion of the plume, which essentially encompasses the first three regions.
The temperature distribution within these regions are influenced by many variables such as location within the plume, discharge channel geometry, discharge water temperature and flow rate, ambient water temperature, elevation, turbulence level, and velocity, lake shcre and bottom configuration, and atmospheric conditions.
1.4.1.1.1.2 Possible Solution Methods A number of theoretical models exist to describe a surface jet discharge. For example, Mot: and Benedict (1) formulated a two dimensional model. However, the two dimensionality of the model results in neclect of jet spreading du Stolzenbach I
and Haricman (2) and Shirazi and Davis (g)to
" buoyancy.
have formulated three dimensional models for deep receiving waters. However, these ggg 1.4-1 l
O formulations cannot be used past the entrainment region due to their underlying assumption that jet mcmentum is much greater than ombient momentum. Also, their predictions are not accurate for shallow receiving waters. 1: hen one considers the complexity of the thermal plume and the many variables which affect it, it is not surprising that a general theoretical model does not exist which will give accertable predictions of the thermal distribution in a shallow receivina basin, such as the nearshore region of Lake Ontario, due to a surface 3et discharge of heated water.
An alternative to the use of a theoretical model as the chief predictive tool in determinina the effects of the Ginna discharge is an empiric Examples o#
of Pritchard,l"})model.Asbury
' and Frigo,151pmpirical modelsand Shirari.IE)are Such those models have the advantage of being based upon actual field measurements of surface jet discharges, thereby implicitly accounting for all of the governing mechanisms. However, their disadvantage is related tc their advantage. That is, since al?
of the mechanisms governing plume behavior are implicitly accounted for, extrapolation of these formulations to sites not similar to those used to derive the formulations is not good practice. This is because the relative magnitude of the varicus mechanisms may be entirely different at different sites.
It should be clear from the above that the best method of predicting the effects of a discharge is to uce a formulation based upon direct field measurements. In this light, extensive data are available for the R.E.Ginna Nuclear Fewer Plant surface jet discharge. Therefore, an empirical model based upon these extensive field measurements will be developed. This model will then be used to assess the effects of the Ginna discharge.
1.4.1.1.1.3 other Empirical Podels A number of empirical studies of surfac iet discharces are available in the literature. Pritchardg47 used data ~ frcm a number of sites along the Great Lakes to arrive at an algorithm for drawing surface isotherms. This model, however, is quite arbitrary in that the chief dependent variables are channel width and discharge temperature. No functional dependence is included for such basic factors as discharge flow, discharge Froude number, etc. The model is applicable to the original data base because the governing factors vary over a fairly narrow range. The plants studied were relatively low capacity fossil fired units with low velocity discharges. The use cf this model for the Ginna plant would be inaprropriate.
Asbury and Frigo (5) also studied various Great Lakes sites to
(} arrive at a relation between dimensionless excess centerline 1.4-2
O temperature, and the ratio of isothern area to discharge flow, I/Co . It is obvious, however, that the latter parameter has the dimensions of inverse velocity. If two data sources have different length scales, the same temperature rise, and equivalent Freude nunbcrs, the latter being required if the near field jet behavior is going to be the same at the two sites, then the ratio of their isotherm areas would be proportional to the square of the ratio of their length scales while the ratio of tnelr flows must be proportional to the 2.5 power of the length scale ratio. Therefore, it would be incorrect to use the parameter I/Qo for data sources other than those from which the relationship was derived.
Shirazi(6) investigated the centerline temperature excess and plume half width of a number of data sources. He took a purely statistical approach and assumed that c
and = a' R,c'F A e' o '
(y) o o h) o where: $T c
= centerline temperature excess, F STg = discharge temperature excess, F r
h = plume half width, ft h = discharge depth, ft o
a = distance along plume trajectory, ft R' = ambient velocity / discharge velocity = Ua /U g F = densimetric Froude nunber = U g 1 ghg ( #a - #o)
Pg l
A = aspect ratio = W/h g a,
= angle between discharge and ambient velocities, radians U
a
= ambient velocity, ft/sec l
Ug = discharge velocity, ft/sec l g = gravitational acceleration, ft/sec O
1.4-3
i O
W = discharge channel width, ft P = ambient density, lb/f t a
p g = discharge density, 1b/ft 3 and a',b',c',d',e',f' = correlation constants which are different ATc r h
for and 6T h o
o Stefan, et al II investigated plume effects within the core region and slightly beyond and found that
- d'-e'T aF hg
=
(a'-b'T)c' 3 exp ( _ g . g. ) 9 (2) where: T = AT c OIo
= dimensionless centerline temperature excess and g',h',i' = correlation constants resulted in a good fit to the data for 1 O s A $ 9.6, 0 $ R's 0.41, 2.0 SF $15, and 0.8sT $0.98.
O 1,4-4
O 1.4.1.1.2 Analytical Discussion 1.4.1.1.2.1 Describing Parameters The effects of a surface jet discharge are influenced by many variables. In the near field these variables can be reduced to the dimensionless parameters F,A,R',K k/p where k = surface heat (where g = OF ,C UEs 8c and C = specific heattransfer coefficieng,)Etu/ft of water, Btu /lb- F , and a for a deep receiving water body. For a shallow recciving water body, the effect of lateral and bottom boundaries mus.t also be considered.
Ambient turbulence is considered to have secondary importance within the near field. (2)
The heat loss parameter, K, can always be neglected in the near field for practical purposes. (E) This can best be i]lustrated by a sample calculation. Using Figure 1.4-29 which shows the expected spring surface isotherms, and taking a value of k = 92 Btu /ft2 _ cf - day, an average value for Lake Ontario,I the heat lost through the surface of the plume to the atmosphere was calculated. It was fcund that less than 3 percent of the heat rejected to the lake by the plant was lost to the atmosphere within the 20F isotherm.
R' and its associated parameter a have not been measured at Ginna.
This is net considered to be a se9ious deficiency in this case.
A surface jet in the presence of a crossflowing ambient will exhibit a distortion of the lateral temperature profiles.
However, if R' is much less than one, the effects of the cross-flow on the plume temperature distribution will be small. The major effect of the crossflow will be a gradual bending of the jet trajectory.(8) At Ginna the discharge velocities are in the r6nge of 3-5 ft/sec., an order of magnitude larger than the currents normally occurring on Lake Ontario. Therefore, the effects of lake currents are expected to be small. It is important to realize that if lake velocities larger than normally expected were to occur, the plume would exhibit greatly increased entrainment rates and, therefore, a much greater rate of temperature decay. (8,10) Hence, at large lake velocities where the crossflow becomes important, its effect is to significantly decrease the size of the thermal plume. on these bases, the parameters R' and a c are not considered further.
A linear scaling factor must be defined so that the plume parameters 7
s,rh,an 61,the Shirazi andisotherm area,can Stefan, et al (') be described used in dimensionless the discharge depth, h form.
Inspection of their general functional forms, equations 1 an8 2, shows that the discharge flow, O g = Ug a, where a = cross section 1.4-5
O area of discharge flow, is accounted for through the use of the variables F,A, and the scale factor h . However, a better choice of length scale would be Va/2. Use of this factor in the formula-tion will reduce the dependence of plume behavior on the aspect ra tio, (2 ) the aspect ratio no longer being necessary to define the size of the discharge.
1.4.1.1.2.2 Centerline Temperature Excess As described in Section 1.4.1.1.1.3, Shirazi(6) described the dimensionless centerline temperature excess, T, as the product of the describing parameters raised to constant powers, as shown in equatien 1. For a specific set of lake and discharge conditions, this equation form reduces to a straiaht line when log T is plotted against log (s/h o ). Figure 1.4-1, which describes the centerline temperature decay at Ginna based on some early field measurements, is such a plot. Note that the curves defining centerline temperature decay are not straight lines.
Rather than h , ya/2 has been used as the scalc factor. For a specific set 8f conditions, use of h e would result in a translation of the curves without changing their shape or slope. As is obvious, the functional form used by Shirari to describe the dependence of T on the distance along the plume trajectory, X, is not O appropriate for Ginna.
The form used by Stefan, et al I was also concidered. Although this formulation was derived only for 0.8 iT CO.98, it was thought that the same functional representation, equation 2, might be applicable to the entire range of temperature excess. As discussed previously, the value of R'can be considered to be essentially zero for this study. Therefore, equation 2 becomes:
d'-e'T S
h
= (a '-b ' T) c ' 3 y, c'F-h',I) exp (i (3) o .
Using becomes Ta/2insteadofhg as the linear scale factor, equation 3 d'-e'T X= = (a'-b'T)c' 3 y,g'F-h',F)exp (i (4) ja/2 . ,
O l
1.4-6
e where: X = dimensionless distance along jet trajectory and a',b',c',d',e',g',h', and i' may have different values than in equation 3.
The function describing the effects of Froude number, the term icated. The values of in brackets in equation 4, was inves+l7) g',h', and i' found by Stefan, et al were 0.5, 1.5, and 0.4 respectively. However, this Froude number function is very difficult to work with statistically in that it cannot be linearized.
Therefora, a new function is sought which would reproduce the
+ sic characteristics of Stefan's function but would be easier manipulate. The first attempt would obviously be Shirazi's o etion, f (F) = a'F (5) where: f (F) = functional dependence of T on F.
However, as is quickly obvious, equation 5 is a monotonic function, whereas Stefan's function, f (p) ,y+ g'F-h' (6) exp (l'F)
O has an extremum located at, i'h'+a' F = (7) i'g' The required functional form of f (F) must, therefore, also have an extremum. A possible function can be deduced from Shirazi.
If equation 5 is expressed in a slightly different form, f (F) = exp (a"+b' In F) (8) where: a" is a new correlation constant, then an extension of this can be postulated as, 2'
f (F) = exp a' + g' ln F+ y' (in F) , (9) e 1.4-7
O where: a', g', and y' are new correlation constants. .
Using the values of g', h', and i' found by Stefan, the method of least squares, which will be explained in Section 1.4.1.1.4, was used to find the best fit of equations 5 and 9 with equation 6 for the range of Froude numbers spanned by the Ginna data.
As will be shown in Section 1.4.1.1.3, this range of F is from approximately 3 to 13. Figure 1.4-2 graphically shows the compari-son between these functions. As expected, equation 5 is a pocr substitute for equation 6, wnereas cquation 9 mimics the charac-teristics of equation 6 quite well.
If equation 9 is substituted for equatien 6 in equation 4 then the equation describing the centerline temperature excess becomes, d'-c'T X= (a'-b'T)c' 3 c'* '
F+ y' F) (10)
The use of aspect ratio as one of the describing parameters in equation 10 cust be examined further in light of the present study. The aspect ratio is defined as, A = W/h g (11) 9 However, the Ginna data is derived from a single discharge with a constant channel width, W. On the other hand, the discharge depth, h , varies directly with the lake elevation. Therefore, any chan,ges in aspect ratio are directly related only to changes in lake elevation, or lake depth. If A were used to describe the thermal distribution at Ginna, it would not be known whether plume charges were due to variation in lake elevation or aspect ratio. In a shallow body of water, changes in lake water depth may result in changes in thermal plume behavior due to a variation in the characteristics of plume interference with the lake bottom.
The phenomenon of plume interference with the lake bottom does not occur in deep water bodies. The latter case was the one investigated by Stefan, et al, (7) and therefore the use of A as a describing parameter did not lead to any uncertainty in model interpretation. In this case, however, model interpretation will be aided by determining whether the variation in lake water depth or aspect ratio is the controlling mecnanism. Model results, of course, depend only on knowing the effect of lake elevation on the plume and not on knowing which mechanism is controlling.
As described previously in this section, the use of ic/2 as the scale factor for length, rather than h g , as used by Stefan, reduces the dependence of the plume description on the aspect ratio. Stolzenbach, et al(12) found that the governing equations k
l 1.4-8
- - - - - - - - - _ _ _ _ _ , _ _ _ _~__
1 I
i Ih outside of the core region in a deep receiving water body are only dependent upon a modified densimetric Froude number, F',
where,
-k {
i F' = FA (12)
This indicates mat plume characteristics are insensitive to changes in asp ratio as compared with changes in Froude number. Since tne effects of aspect ratio variations are known to be small, a significant effect of lake elevation on the plume can only be interpreted as signifying that lake depth varia-tions are the controlling mechanism.
The parameter describing lake water depth can be taken as lake surface elevation minus an effective lake bottom elevation which would result in a similar thermal distribution as the sloping bottom at Ginna. In order to reduce this parameter to dimensionless form, the length scale f actor, y a/2 , might be considered.
However, since changes in channel cross section area, a, are due solely to changes in lake water depth, the use of ya/2 as a scale factor would effectively be the same thing as considering the square root of the lake depth as the dimensionless parameter. g This,4cf course, is no longer dimensionless, having the dimension of ft-W
. A better choice as scale factor would be the average lake depth. This value is independent of the instantaneous lake depth. Therefore, in place of aspect ratio, a dimensionless lake depth is used, which is defined as, E-b D= _ (13)
E-b where: E= lake surface elevation, ft b = effective lake bottom elevation, ft E = average lake surface elevation, ft D = dimensionless lake depth The use of D rather than A as a describing parameter leaves in question the appropriate functional form to be used in describing thecenterlineexcesstemperatureofthegpume. The functional form of the aspect ratio used by Shirazi( was,
=A U'
f(A) (14) where f (A) = functional dependence of T on A. Stefan, et cl U)used, 1
1.4-9 l
l t
O f(A) =A d'-e'T (15)
The lake depth, or plume bottom interference, will have a varying effect along the length of a thermal plume. Initially, the plume would not interact significantly with the botton. As the water is transported further frem the discharge, turbulent shears induced by the discharge jet momentum would tend to deepen the plume, thereby resulting in greater 'o+. tom interf erence. As the dischart . momentum was dissipated, yant forces would cause the plume botten to rise of f the la) Therefore, the functional form describing the dependence mt possess the charac-teristic of an extremum at some >tueen 0 and 1. An _
extension of equations 14 and 15 .. form, ny +n,' (T-1) +n 3
M4 f (D) =D (16) where: f (D) = functional dependence ci T on n y,n = correlation constants 2 '"3 and T-1 is used in place of T so that the value at the end of the core region, Tal, is readily apparent. The use of T-1 rather than T does not change the function but does change the correla-ggg tion constants.
Substituting equation 16 for 15 in equation 10 results in,
+n X= (a'-b'T)c, Dny+n3(T-1) ' 3(T-1)2 exp a' + g'In F+ P' (In F ) (17)
Equation 17 was investigated with respect to the major temperature dependence, f (T) = (a'-b'T)c' gy g) where: f(T) describes the major interdependence of T and X .
This functional form, although adequately describing the shape of the Ginna data found in Figure 1.4-1, is statistically very difficult to work with due to the impossibility of expressing it in linear form. Also, as described in Section 1.4.1.1.3, less than 1% of the Ginna data has dimersionless excess centerline temperatures greater than 0.8, the lower limit of the range of Stefan's data. Equation le was used to fit sample data for T<0.8.
It was found that b' > a ' . Therefore, f (T) in equation 18 is negative for T=1. This, of course, is physically unrealistic.
The dual problems of physical realism and difficulty cf manipu-lation required a different function than that given in equation 18.
1.4-10
In earlier parts of this section, the inadequacy of Shirazi's(6) functional form, which can be derived from equation 1 as, b'
f (T) = a'T gg) where a' and b' are the inverses of the correlation constants indicated in equation 1, was discussed. Equation 18, on the other hand, does provide a clue to a convenient and realistic function.
c', c' was Rather than using a'-b'T as the base for an exponent used as a base for the exponent a'-b'T. This can be expressed as, f (T) = c,a'-b'T (20)
Equation 20 can be transformed to, f (T) = exp p' + @' (T-1) (21) where: p' = (a'-b')ln c'= new correlation constant
= -b' in c'
@' = new correlation constant and a',b' and c' are the values appropriate for equation 20. Note that one less correlation constant is necessary for the description f(T) in the form of equation 21 than is required in the form of equatien 2 0. As in equation 10, T-1 is used rather than T so that the value cf f (T) at the end of the core region is readily calcul-able.
Unlike equation 18, equation 21 has the advantage of always being positive at the end of the core region . This is readily apparent by substituting T=1, the definition of the end of the core region, into equation 21. The result is f(T) =e at T=1 (21a)
This function is greater than zero for any value of p'.
t l Equation 21 has the additional advantage of being readily expanded to include higher powers of T-1. For example, f(T) = exp p + @(T-1) + 6 (T-1) (22) p", 0, and 6'are correlation constants,
~
where:
might be used to improve the fit of equation 21 to the data.
For illustration purposes, the method of least squares, which will be explained in Section 1.4.1.1.3, was used to determine 9
1.4-11
imm l
O the constants of equations 21 and 22 so as to provide the best fit to the worst case, surface curve of Figure 1.4-1, which shows the actual trend of the Ginna data. Figure 1.4-3, is a graphical depiction of the results. It is seen that both equations 21 and 22 are good representations of the data, but, as expected, equation 22 is a slightly better fit.
Replacing equation 18 with equation 22 in equation 17 results in, n y +n, (T-1) +n3 (T-1) '
X = exp $"+ @ (T-1) + 6 (T-1) D (23) x exp a ' + S'in F+ y' (in F) '
~
Equation 23 can also be expressed as,
~
, n,+n,(T-1)+n3(T-1) ya exp p+ $ (T-1) + 6 (T-1) ' D* '
(24) x exp g'In F+ y' (In F) where @= @"+ a' of equation 23 = new correlation constant.
[}
Equation 24 represents the general forn used in this study to determine the dependence of temperature excess along .he rivue centerline on lake elevation and Froude number. The .awrtc depends on discharge velocity, which, fcr a constant discharge flow rate and channel width such as exists at Ginna, depends only upon lake elevation, discharge flow depth, which also depends only on lake elevation at Ginna, and (p-p for a constant excess discharge temperature, dehen8s) / p , which,o61y on lake temperature. Therefore, for a constant discharge excess temperature, equation 24 actually shows the effects of varying lake elevation anc lake temperature on the centerline excess temperature of the plume, 1.4.1.1.2.3 Plume Half Width The plume half width, r,h is a convenient parameter for describing the manner in which the plume spreads. Shirazi(6) assumed that the same functional form describes plume half width and centerline temperature excess. However, Figure 1.4-1 indicates that the functional form describing the dependence of r s on s is quite different than the form of T versus s indicated in equation 21 or 22.
Engelund and pederson Il I develcped a semi-empirical model to
() describe the temperature distribution near the discharge point 1.4-12
O of a high Froude number surface jet discharging into a deep, stagnant water body. Edinger, et al (14) reduced the work of Engelund and Pederson into two possible surface distributions of excess temperature, AT 12 6T =
c exp 14 F
2 Ir l X -14/3 oT 3 oT o 3 kj'a/2/ (25) and . 7 ,
6T 6To e
6T o pM F 2
[ r y-14/3 (26) 9
( j'a/2 / ,
where: r = plume width at excess temperature 6T and dimensionless longitudinal distance X, ft and 6T = excess temperature at location (X , r) , F If 6T is taken as one half 6T , then r=r in equation 25 and 26 c h by definition.
If equations 25 and 26 are then solved for r h
the results are, O F
r 0.5 = 0.67 x and r 0.5 = 0.80 X F (28) where r 3 =rq/ j'a/2 = dimensionless plume half width. Equations 27 and kB correspond to equations 25 and 26 respectively.
Equations 27 and 28 can be seen to be similar in form to Shira::i's function; that is, r.5=a'X 0
F (29) where a',b' and d' are correlation constants different than those of equation 1.
Equation 29 differs from equation 1 in that no functional dependence is present fcr R, a', and A. R and a' are not included because Engelund and Pederson considered a stagnant receiving water. As discussed near the beginninc of this section, r may be taken as independent of R and a' for the present studh:5 That is, from O
1.4-13
O the staadpoint of plume dilution at Ginna, Lake Ontario may be considered as a stagnant body of water.
The aspect ratio, A, was thoroughly discussed in Section 1.4.1.1.2.2.
It was shown that D, the dimensionless lake depth, was a better variable to consider than A for a shallow receiving water body such as Lake Ontario at the Ginna site. However, experimental data (2,8 ) has shown that the plume half width does not depend upon the receiving water depth. Therefore, it is expected that r will depend nly n X and F in a manner similar to equation 29.
0.5 Note that the plume half width curves of Figure 1.4-1 would be straight lines if equation 29 were a proper description of the Ginna data. Since they are not, the functional form of equation 29 is extended in a similar manner to the extension of equation 8 into equation 9. The resulting equation, which includes a possible lake depth dependence is, r0.5=exp Qin X + y (in X ) hn F H (in F) UnD (30)
Note that the functional form of D is not as complicated as the form for X and F. This is because, as explained previously, g r is not expected to depend on D. If the data verifies this, tSe last term in equation 30 will be dropped. If the analysis of the Ginna data shows otherwise, the functicnal form of D can easily be expanded into a form similar to either equation 9 or equation 16, 1.4.1.1.2.4 Lateral Distribution The lateral excess temperature distribution in a surface jet dgschgrg,glume
( ,6, 4) is usually assumed to be Gaussian in form.
In those cases where other forms are used, (2,13) the resulting distribution does not vary greatly from that which would be given by a Gaussian relationship.
The lateral temperature distribution at Ginna will therefore be expressed as, _
Tg = n exp -p(r/r ) (31) h m = 6T / ATc where: T = dimensionless lateral temperature at r n and p = constants and r and r h are as defined previously. Outside of the core 1.4-14
region, r must be 0when T = 1. Also, by definition, r must O
equal r when T =0.5.
m Sub9tituting these conditions into equation 31, and 3 solving for n and p results in, n=1 (32) p = In 2 = 0.693 The use of equations 31 and 32 does not allow for any variation of the postulated distribution which may be inherent in the Ginna data. However, data variations can be accounted for by assuming that separate distributions be calculated for the ranget.
0.55 T 4 1 and T_4 0.5. If equation 31 is used for both ranges, then iE has been"shown previously that equations 32 must hold for 0.55 T,5 1. However, the distribution for T 4.0.5 requires only that Y=r when T =0.5. Substitutino this criterion into equation 31 abd solvi9g for n in terms of p results in, n = 0.5 exp(p) (33)
If p=ln 2 then equation 33 is equivalent to equation 32.
The lateral distribution for this study is therefore taken as equations 31 and 33. The equation set 32 is noted as a special case of equation 33. h O
1.4-15
l.4.1.1.3 Data Description
() 1.4.1.1.3.1 Data Collection Rochester Gas and Electric Corporation has an extensive field survey program for collecting lake temperature data in the vicinity of the Ginna discharge. During surveys, temperatures are continuously recorded from thermistors at four different depths along a grid pattern which is traversed by boat. Figure 1.4-4 shows the survey transect locatiens, bearing lines, and nine site-alignment target locations. The boat follows the bearing lines, its passing a transect intersection being noted on a multichannel strip-chart recorder. A pass is also made between intersections 14 and 20 to determine the fine structure of the plume in the region near the discharge. Ambient tempera-tures are determined from offshore thermal measurenents outside of the plume area. When no horizontal thermal oradient is measured, ambient temperature is considered to have been sampled. The measured data are converted into isotherm plots at each depth.
The surveys are performed approximately monthly, except during winter months and periods of plant shutdown. See Table 1.4-10.
1.4.1.1.3.2 Data Range The above described isotherm plots for the period from the middle of 1970 to the middle of 1975 served as the data source for this analysis. As described in Section 1.4.1.1.2, the tenperature
() excess at various locations within the plume will be functions of F, the densimetric Froude number, and D, the dimensionless lake depth. The latter variable, however, depends only upon the lake elevation, E.
In order to determine the Froudn number, the discharge temperature, ambient temperature, and lake level, or discharge depth, must be known. The former two variables are measured by RG&E. Lake levels were obtained from NOAA(15) records for the Rochester gaging station. The levels used were the daily means reported by NOAA for the dates of the thermal surveys. For consistency, Froude numbers were calculated using the ambient temperature at the lake surface. Table 1.4-2 lists the survey dates and their associated values of F and E. Figure 1.4-5 is a graphical interpretation of Table 1.4-2, each point representing one survey. The figure shows that, although F ranges from 2.87 to 12.88, most of the data lie between 3.5 and 10. The elevation data, in feet USGS, range from 244.90 to 249.25, with the major cluster lying between 245 and 247.
Two survey dates, 3/19/70 and 3/30/72, were available but were not used. The ambient water temperatures in these two cases were 33 F and 340F, respectively. Due to the fact that water density reaches a maximum at 39.20F, the thermal plume will sink below the lake surface rather than remain at the surface for low 1.4-16
excess temperatures. This plume cehavior can not be described in O
the same way as buoyant plume behavior. Therefore, these two dates were not used as part of the data base for this study.
1.4.1.1.3.3 Surface Data Reduction Once the describing parameters F and E were found for each date, the thermal plume behavior for the corresponding survey was characterized. This was done by examining the appropriate surface isotherm plot (the surface data were actually taken at a depth of 0.5 feet) and determining the plume ;enterline by drawing a smooth curve through the vertices of the isotherms. The plume centerline in the plane of the isotherms defined the s coordinate.
Centerline temperatures were read at values of s corresponding to isotherm vertices. Centerline excess temperatures were determined by subtracting the field measured lake ambient temperature. Plume half widths were found corresponding to the s coordinates of isotherm vertices whose excess temperatures were multiples of 2.
In this way, actual isotherm boundaries could be measured, thereby eliminating any need for determining half widths from interpolated values. The centerline temperature excesses were then scaled to the discharge excess temperature, while s_and_rb were normalized to Ta/2. The resulting dimensionless values defined the temperature decay and spreading characteristics of the plume.
Table 1.4-3 is a reproduction of the computer printout giving the data obtained by the methods described above. In this table, DT=date, FR=densimetric Froude number, ELEU= lake elevation in ft USGS, NO. PTS (CL)= number of centerline excess temperature data points for that date, NO. PTS (RHALF) = number of half width data points for that date, X=dimensionless longitudinal distance, T= dimension-less centerline excess temperature, and REALF=dimensionless plume half width. A value of PHALF=-0.0 indicates that the plume half width at the corresponding longitudinal distance was not reduced.
The bottom of the table shows that 425 centerline excess tempe-rature data points and 197 half width data points were reduced at the surface. Figures 1.4-6 and 1.4-7 show typical data for the dates 9/25/70 and 10/27/71 in the same graphical form as Figure 1.4-1.
1.4.1.1.3.4 Subsurface Data Reduction Temperature surveys at Ginna show that the thermal plure rarely goes below 9 or 10 feet. Therefore, the temperature distribution at a depth of 6 feet was used to describe the subsurface thermal effects. The surface and 6 foot isotherms describe the three dimensional aspects of the thermal distribution at Ginna.
O 1.4-17
_- .- . . . . - ~. - - - - . - .- -. . - . - - -
O Subsurface temperatures over the 5 years cf data were sampled at various depths. Therefore, lake depths of 6 feet 113 inches were nominally identified as 6 foot data.
Some of the survey dates did not include subsurface isotherms within the indicated depth range. Others had to be neglected due to anomalies in the isotherm patterns. This left 32 of the 43 surveys to form the subsurface data base for this study. Table 1.4-2 shows the dates and depths of those surveys that were used to indicate the subsurface behavior of the plume. A dash in the Subsurface Isotherm Depth column indicates a survey that was not used as input to the model.
The subsurface isotherms were measured and reduced in exactly the same manner as the surface isotherms, except for the determination of ambient. temperature. In order to achieve the most realistic analysis of the Ginna data, any vertical lake temperature stratifi-cation was accounted for by taking the ambient temperature as that indicated in the appropriate isotherm plot rather than that measured at the lake surface. Table 1.4-4 gives the data reduced in the manner described above. The headings for this table are the same as those given for Table 1.4-3, the surface data listing.
259 centerline excess temperature data points and 111 half width data points were reduced. Figures 1.4-8 and 1,4-9 show typical
() plots of the data for 5/1/70 and 10/1/73.
1.4.1.1.4 Statistical Methods and Resulting Equations 1.4.1.1.4.1 Statistical Methods In order to mathematically describe the Ginna data, a relation must be established between the data and the describing mathe-matical expressions.- An often used method is the method of least squares.
The criterion describing the relationship between the data and the describing mathematical expression is, m 2 must be a minimum, 5 =}[ e g (34) i=1 where m = number of data points th data point and the 31 = value difference between the i of the mathematical expression at that i
point; that is, the error of the mathematical expression at data point i
(]) and 5 = sum of the squares of the errors.
1.4-18
This method determines the coefficients of the mathematical O
expression such that the sum of the squares of the errors are minimi ed. A necessary and sufficient condition for equation 34 is,ll6)
B5 Ba.
= 0 (35) 3 where: a. = the correlation constants which define the 3
describing mathematical expression.
Equations 35 describe one equation for each correlation constant that is to be determined, thereby uniquely defining the solution.
If the describing mathematical expression is linear in the correlation constants, equations 35 define a system of simulta-neous linear equations. The solution to such a system is always obtainable. On the other hand, if the mathematical expression is nonlinear in the correlation constants, equations 35 must be solved by numerical iterative techniques. If the number of equations are large and the form of the equation is complicated, the numerical iterative techniques will not always converge to the solution. (17) It is for this reason that equation 9 is preferred to equation 6 in describing the Froude number effect on centerline temperature excess, asdescribedinSection1.4.1.1.2.ll l 1.4.1.1.4.2 Centerline Temperature Excess As shown in Section 1.4.1.1.2, equation 24, which is repeated below, represents the expected form of the relationship among the dimensionless centerline distance, x, the dimensionless centerline excess temperature, T, the dimensionless lake depth, D, and the densimetric Froude number, F.
~ ,
f ny+n 2(T-1)+"3(T-1)^ ~
9 X = exp 6+ p (T-1) + 6 (T-1) ' D expfT in F+ P' (In F) ' (24)
As described in the discussion of statistical methods, it is advantageous to express equation 24 in such a way that the resulting equation is linear in the correlation constantsp, @, 6 ,
n y,n,,n,, S', and y'. Such a transformation may be accomplished by taking the natural logarithm of both sides of equation 24.
The result is, in x=9+ $ (T-1) + 6 (T-1) +ny ln D+n2 (T-1)ln D+n2(T-1) in D+$'In F+ P' (In F) (3 0
1.4-19
The final determination of the equation describing the Ginna data proceeded in steps. The first step involved determining how well the basic x , T relationship fit the data. The goodness of it ofthemathematicalformulatothedatawasdeterminedby,I{8)
~ ~ '
m 2 m
[ Y ~5 i
[ Y -h i i R= i"I (37) m ,
Yi '5 i=1 where:
m = number of data points y1 = the data point in X g 9u average value of inx for the m data points
$ 1 = predicted value of in xg and R = correlation coefficient.
As can be seen from examining equation 37, R represents the
() success of the mathematical formulation to predict the data as measured against how well the average of the data describes individual data points. If the mathematical fcrmula is an exact description of the data, R=1. If the formula is no better than using the average of the data, R=0. Therefore, the better the description of the mathematical formula to the data, the greater will be the value of R.
After the correlation coefficient was determined for the basic x ,T relationship, in x = p + @ (T-1) (38) additional terms in equation 38 were investigated. For example, in x = p + @ (T-1) + 6 (T-1)' (39) was next investigated. It was found that this additional term resulted in an insignificant improvement in the data fit. The functional dependence of F on the centerline excess temperature was next investigated by first considering, in X = @+ @ (T-1) +S' In F+ y' (ln F) * (4 0) 1.4-20
and then considering, llh in x= 9+ @(T-1)+p'In F. (41)
It was found that the addition of the Froude number dependence to equation 38 resulted in an insignificant statistical advantage for the surface isotherms. Howe'er, equation 41 was seen to provide an improvement in the correlation coefficient for the 6 foot depth isotherms, althouah equation 40 was no inprovement over equation 41.
The effect of dimensionless lake depth, D, on the excess centerline temperature was investigated in a manner similar to the investi-gation of the densimetr.c Froude number. It was found that the effect of D on the Ginna isotherms was small. After determining in this way that equations 38 and 41 represented the centerline temperature excess at the surface and 6 feet, respectively, the complete form of equation 36 was checked to see if any synergistic effects existed. The correlation coefficient was found to be substantially unchanged. The final equations, therefore, that were used to describe the ccnterline temperature excess at Ginna were in X = @ + @ (T-1) , at the surface (38) and in X = @ + @ (T-1) +$'in P, at 6 foot depth (41)
O The constants @and @are, of course, different for the two depths.
The values of R for the surface and 6 feet are, 0.784 and 0.746, respectively. The standard deviations, a , of the independent variable, in x , at the two depths are, 0.351 and 0.374, respectively.
Table 1.4-5 summarizes the correlation constants and associated statistical data for the surface and 6 feet.
The form of equation 38 shows that the excess centerline temperature at the surface of the Ginna thermal plume is unaffected by the Froude number and dimensionless lake depth over the range of the Ginna data. This typ of behavior was observed by Jen, et al ,(19 )
and Engelund and Pederson 13) both of whom found that the excess centerline temperature at the surface was dependent only upon gbe distance from the discharge for large Froude numbers. Shirazi}b on the other hand, reports a Froude number dependence, although it is not known whether he investigated the statistical signifi-cance of this dependence.
The six foot depth excess centerline temperatures were found to to be affected by the Froude number, although not affected by the dimensionless lake depth except as that variable affects the Froude number. As the Froude number increases, the subsurface centerline O
l 1.4-21
O temperature excess increases. This is expected because an increase in Froude number indicates that the inertial forces increase relative to the buoyant forces. This implies that the plume bottom does not rise until later in its developnent. The higher the Froude number, the longer the plume remains in contact with the six foot depth ambient water. As the Froude number decreases, the longitudinal distance at which the thermal plume separates from the six foot contour decreases. This heat rises to the surface, causing plume spreading to increase, as will be shown in-Section 1.4.1.1.4.3.
The statistical results given in Table 1.4-5 show that the mathematical nodel is a better representation of the surface data than of the six foot data. This reflects the fact that the six foot data actually represents lake depths between 4'11" and 7'1",
whereas the surface data were always at a depth of O'6".
Figure 1.4-10 shows xys T for the lake surface. Figure 1.4-13 gives the same information for six foot depth.
1.4.1.1.4.3 plume Half-Fidth The expected forn of the plume half width relationship is, O -
(in r0.5=exp a +$in x + y (In x ) 2+ S in F+ t (in M (30) as shown in Section 1.4.1.1.2.3. As described in Section 1.4.1.1.4.1, a form of this equation which is linear in the correlation constants , a , S , y , S , c , and ( , is preferred. Such a form can be obtained by taking the natural logarithm of each side of equation 30. The resulting equation is, in r 0 5= a + Sin x + Y (in x ) 2+ 6 in F+ f (In F) +(ln D. (31)
As in the case of the centerline temperature excess determination, the basic r0.5, x relationship was determined from in r . 05= a + Sin x . (42)
The effect of adding the term in (In' x ) vas then studied. It
! was found that this effect was significant. The addition of-l the terms describing F were investigated by studying first, In r0. 5= a + Sin X + Y(in x ) 2+ S ln F (4 3)
O ,
and then, in r0.5=a+ S 3 n x + Y (in X ) +61n F +((ln F)~. (44) 1.4-22 4
O It was found, for both the surface and subsurface data, that equation 43 resulted in a definite improvement in the fit to the data, but no further3deprovenent was gained through the additien of the term in (in F)', equation 44. The term in in D was then considered and found to be statistically unjustifiable. The complete equation 31 was then tried and the correlation coeffi-cient was found to be essentially the same as for equation 43.
Therefore, the final form of the plume half width equation was taken as, in r0. 5= a + Sin x + y (in X ) '+ 61n F, (43) for both surface and six foot depth isotherms.
The correlation constants a , S , y , and bare different at the two depths and are given in Table 1,4-5. The correlation coefficients, P. , for the surface and six foot depth equations are, 0.647 and 0.600. The standard deviations,o , of the independent variable,ln r , at the two depths are, 0.481 and 0.5 0.570 respectively.
The form of equation 43 indicates that the dimensionless lake depth does not affect the plume half width, except through its effect en the densimetric Froude number. This characteristic was hypcthesi cd in Section 1.4.1.1.2.3 and confirmed by the statistical study. The Froude number behav4 in which 6 gp less than zero, agrees with that of Shirazi)g ,Jen, et al and Engelund and Pederson. (13) In fact, Jen found the dependence of the half width on ghe5 densimetric Froude number at the water surfa The Ginna data shows this dependence as F~ge *g be as F-0.
- 20' .
The fact that the surface plume widths increase with decreasing Froude number was discussed in Section 1.4.1.1.4.2. As the Froude number decr eases, the effect of buoyancy increases. Therefore, the plume rises from the six foot contour more quickly, resulting in greater spreading on the surface. This is exactly the behavior predicted by the centerline temperature excess and plume half width relations.
Figure 1.4-12 and 1.4-13 show the plume half widths as a function of centerline distance and densimetric Froude number. The surface isotherms are seen to have half widths always greater than those at six foot depth, illustrating the effect of buoyancy on plume behavior.
O 1.4-23
i o
(_) 1.4.1.1.4.4 Lateral Distribution As shown in Section 1.4.1.1.2.4, the lateral distribution is expected to have the form, T,=n exp -p(r/r g)2 , (31)
The Ginna lateral distribution can be determined by measuring the r values correspending to the various isotherms at each centerline point where rh has been determined. Such an under-taking, however, would be impossible to complete within any reasonabic time constraint due to the large number of r values which could be measured (from 3-15 points must be measured for each rh). Instead of considering all 43 surveys, five surveys were chosen for the lateral distribution analysis. The survey dates were 5/1/70, 12/1/71, 5/14/73, ll/13/73,and 8/4/75. They were chosen so as to represent the range of lake elevations and Froude numbers experienced by the Cinna discherge.
For each centerline point at which the plume half width was measured, values of n and p were determined for 0.55 TyC1 and Tm50.5 in accordance with equations 31 and 33, the latter being, rS n = 0.5 exp (p) (33)
V Equation 33 results from the fact that r = rp' at T_=6T/AT c =0,5, '"
as shown in Section 1.4.1.1.2.4.
The values of n and p were determined from a least squares fit of the studied lateral distributions, of which there were 23 in the five surveys. It was found that p=0.661 described the distributions for 0.5 < T < 1 and p=0.663 described the distribu-tions for T < 0. 5. As described in the analytical discussion, the fact thEt T = 1 when r = 0 and T =0.5 when r=rh implies that p =ln 2 = 0.693* Table 1.4-6 compares the lateral distributions found from the Ginna data with that of a normalized Gaussian (n=1, p=ln 2). It is seen that, except for values of T near one, the normalized Gaussian is virtually the same as the Ginna distribution. Since it was shown that the normalized Gaussian must apply for the region 0.5 ST C 1, and since the two distribu-tions are almost identical excepE for the small region where T 1, the normalized Gaussian is taken as the appropriate dis =tribution. That is T,= exp -In 2 (r/r h) (4 5) o 1,4 .24 . l
describes the lateral temperature distribution. This distribution is the one most frequently used by investigators of thermal plumes.
(3,6,8,11,14) Figure 1.4-14 is a graphical depiction of the lateral distribution, equation 45.
1.4.1.1.4.6 Possible Sources of Data Scatter Scatter in the cor relation model may result frem either inadequacies in the model or inaccuracies in the data. Inadequacies in the model would stem from neglecting important mechanisms which affect the thermal distribution. The major model assumption was that Lake Ontario currents do not affect the thermal plume except for a gradual bending of its trajectory. Such an assumption was shown to be valid for current velocities much less than the discharge velocity, a condition normally expected at Ginna.
Greater current velocities result in increased mixing with the ambient in addition to the bending of the jet trajectory. Any increase in ambient entrainment was not accounted for by the correlation model. Section 1.4.1.1.2 discusses the other mechanisms which affect the Girma thermal plume.
Data inaccuracies are inherent in any sampling program. The inaccuracies of the temperature measuring devices, inaccuracies in boat position and speed determinations, and inaccuracies in the determination of sampling depth due to the presence of waves cannot be eliminated.
lll A perhaps more important data error source lies in the determina-tion of ambient temperatures and therefore the determination of excess teuperatures. The ambient temperature for each survey 9 However, was obtained by Chermack and Galletta samplir(e 20)offshore found of that the the thermal undisturbed plume. ambient at Ginna always exhibits a horizontal thermal gradient between the shoreline and 5000 feet offshore. When this gradient is positive, as it is from March until August, the Ginna data exce'ss temperatures are overstatements of their actual value. When the gradient is negative, at it is from September until February, the Ginna data excess temperatures are understatements of their true value. Table 1.4-7 shows the monthly temperature difference found by Cheaaack and Galletta between the shoreline and 5000 feet offshore in the vicinity of the Ginna site for the years 1969-1972. It is seen that the yearly average gradient is +0.6 F between these points. Of the Ginna thermal surveys, 60% were sampled during positive gradient months and 40% during negative gradient months. The average gradient between the shoreline and 5000 feet offshore for all of the thermal surveys was +0.7 F, thereby indicating that the overall effect of the horizontal O
1.4-25 I
1
temperature gradient is to make the excess temperature data conservatively high, although the opposite will be true for thermal surveys taken between September and February. In practice, no surveys are taken in January and February, 1.4.1.1.5 Model Application 1.4.1.1.5.1 Isotherm Construction The first step in constructing isotherm maps from the mathematical model is a specification of the ambient conditions. Lake eleva-tion and ambient temperature uniquely determine, for a constant temperature rise, the densimetric Froude number, F, and linear scale factor, ya/2, for a given discharge. The values at Ginna of the latter two carameters may be found from Ficures 1.4-15 and 1.4-16 or calculated directly from their definitions. Note that the densimetric Froude numbers given in Figure 1.4-15 assume the Ginna design discharge excess temperature of 200F. Dimensionless temperature excesses, T, along the plume trajectory,r , are then found from either Figure 1.4-10 or equation 38 for surface isotherms and either Figure 1.4-11 or equation 41 for six foot depth isotherms.
At each location along the plume centerline, dimensionless half widths, r , are calculated from equation 43 or Figures 1.4-12 (surface)0bd1.4-13 a (six foot depth). Multiplication of the
(~} dimensionless half widths and centerline distances by the linear A- scale factor and of the dimensionless centerline temperature excess by the discharge temperature excess,$T, , results in the corresponding dimensioned variables, r s, and AT_ , Use of Figure 1.4-14 or equation 45 then allohs, the calculation of the temperature excess at various distances normal to the centerline for each value of s and the corresponding value of r p and oTc '
Within the core region, T=1, the lateral temperature' profile changes from a constant to Gaussian. 1;o data are available within this region. It can be assumed that the isotherms spread linearly _between the discharge and the end of the core region.
1.4.1.1.5.2 Worst Case Isotherms The surface and subsurface isotherms described in Section 1.4.1.1.5.1 are derived from exeected values of the dimensionless centerline temperature excess and half width. However, due to data scatter, any single measurement will normally not conform to its expected value. This data behavior .can be described by considering confidence limits around the expected value. That is, any single measurement may not conform to its expected value but it will have a certain probability, the confidence linit, of being within a specified range. The probability chosen for the confidence limit is frequently 0.95, or 951. This confidence limit allows one to state with reasonable certainty that a single
()
1.4-26
l measurement will lie within a physically meaningful data range.
If two variables were directly proportional, the probability that both would exceed their 951 upper confidence limit would be the same as the probability that one would exceed its 951 upper confidence limit. If two variables were totally independent, then the probability that either will exceed its 77.6% upper confidence limit is 0.224, but the probability that both will exceed their
- 77. 6% upp er confidence limit is 0.95. Expressed another way, if two variables are directly proportional, their combined 951 upper confidence limit is the 95S upper confidence limit of each; whereas, if two variables are independent, their combined 95%
upper confidence limit is the 77.6% upper confidence limit cf each. Next, consider the case of two inversely proportional variables. The probability that both will exceed their 951 upper confidence limit is virtually zero since as one increases from its expected value toward its 95% upper confidence limit the other will decrease.
In this analysis we are dealing with a case which is intermediate of the latter two cases described in the previous paragraph. As found by all investigators of the thermal plume phenomenon, for a given set of discharge conditions, half widths will always decrease with increasinc isotherm lencths. Indeed, this must be
~
true because a constant heat rejection rate implies a constant plume heat flux. Due to the many factors which affect thermal ll) plume s ,it is not possible to quantift is inverse relationship.
The joint 95% upper confidence limit centerline temperature excess and half width, therefore, cannot be quantified. Eowever, an upper confidence limit can be ascribed to these variables.
If the centerline temperature excess or plume half width were at its 95S upper confidence limit, the other variable should be less than its expected value due to the inverse relationship described above. A 95+1 upper confidence limit (the exact confidence value is not determinable) can therefore be taken as either variable at the upper range of its 95% confidence limit with the other variable at its expected value. The resulting isotherms can be labelled " worst case."
Isotherm areas were calculated for the 95% confidence limit of centerline temperature excess with the expected plume half width and vice versa. Results from the former case indicated 30F surf ace isotherm areas approximately 10% larger than the latter.
Therefore, the former case is used to quantify " worst case" isotherm effects.
O 1.4-27
1.4.1.2 Comparison of Model With Data As explained in Section 1.4.1.1.5.2, an individual measurement may not be equal to its expected value. The measurement must, therefore, be compared with some confidence range, 951 being chosen, rigures 1.4-6 through 1.4-9 show typical surface and six foot centerline temperature excess and plume half width data.
Also shown are the 951 confidence limits corresponding to the ambient conditions prevalent on each date. Note that all of the data lies within the chc4en confidence limits. Figure 1.4-8, surface data on 5/1/70, was specifically chosen in order to illustrate a case where centerline temperature excess data may be near their upper confidence limit. Note, however that the half width data are near their expected values. Most of the other data points are near their expected values, except for a few surface half width points on 10/27/71. !!ere again the center-line temperature excess data are near their expected values.
Section 3. 4 .2. 6 gives che plume size for a wide rance of tmbient ~
conditions. As will be shown there, the worct case plume will 0
have a 3 r surface area : nging up to agproximately 470 acres.
This can be compared witn the largest 3 r area ever noted during the Ginna tt tal surveys of 235.2 acres. The worst case plume will have a area at six foot depth ranging up to approximately
(] 160 acres. i i can be compared with the maximum value actually observed at G. Sa of 120.4 acres. This illustrates the fact that the worst case plume is actually a 95+t confidence limit, as explained in Section 1.4.1.1.5.2. The above figures are exclusive of winter, when tmbient conditions are such that the plume will sink. As explained in Section 1.4.1.1.3.2, the model has not been derived for these conditions. However, winter plume effects are addressed in Section 1.4.2.
As described in Section 1. 4.1.1. 3, Ginna thermal suryny data taken from 5/1/70 t% rough 8/4/75 were used to develop the mathematical model. Eight surveys were performed during the period from 9/11/75 through 11/5/76. These surveys were used as an independent check of the model. Three of the eight surveys had no 30T isotherm existing at the six foot level. Three others had six foot therm 11 distributions which did not emanate from_the discharge, an under-lying assumption of the model. It is of interest to note, however, that these latter three had 30 F six foot depth areas 31, 33 and 92% of that given by worst case-plume predictions corresponding to their ambient and discharge conditions.
The remaining two six foot depth temperature distributions along with the eight surf ace distributions were reduced to dimensionless form in the manner described in Section 1.4.1.1.3. Figures 1.4-17 through 26 show this data along with their associated 95%
O confidence limits. Two half width data points at the six foot depth and one point at the surface lie slightly outside the 951 confidence range on 10/21/75. Nota that the corresponding 1.4-28
I centerline temperature excesses are near their expected value. l These large half widths can be attributed to uncertainty in )
determining the plume trajectory. A different plume trajectory l would recult in different values of the dimensionless variables. !
A number of centerline temperature excess data points at high excess temperatures are less than the low end of the 951 confidence range. These, together with the three surveys which showed no 30F excess temperatures at six foot depth, is evidence suggesting that the model may be somewhat of an overstatement of the thermal plume size at Ginna. If the curveys performed subsequent to 8/4/75 were integrated into the model, predicted isothermal areas would probab.ly be somewhat smaller than those given in this study.
O 1.4-29
1.4.2 THEPRAL ErrECTS Or DISCHARGE 1.4.2.1 Ambient condi+. inns l 4
i As explained in Section 1.4.1, the temperature distribution ;
resulting from the Ginna discharge will depend upon the lake elevation and lake temperature. Lake elevations were obtained from the daily records of NOAA's Rochester gaging station for the period frem January 1953 through Deecmber 1976.(15) Lake temperaturen were determined frem the daily records of the Ginna intake water temperature for the period from January 1970 through November 1976.
Seasonal elevation's and temperatures were determined from the >
4 daily records. The winter, spring, summer, and fall seasons were 4 taken as consecutive three month periods beginning with January. '
Table 1.4-8 gives the seasonal lake temperatures and elevations. ,
1.4.2.2 Lako-Bottom Tenperature Rise !
In-May 1974, RG&E sponsored 3 field surveys to determine discharge induced lake bottom temperatures and velocities at the Ginna site. (See Section 1.4.3.1.2 for a discussion of betteu velocities) . '
Excess temperatures and associated areas from these surveys were nondimensionalized in a manner sinilar to that described in O Section 1.4.1.1. The relationship between excess temperatures and areas, for the conditions existing while the measurements were being performed, was found to be, A, = -18.86 f-o + 9. 4 9 (46) and A,= -20.T2 0 +13.35, (47) ;
where A 8
= area of isotherm whose excess temperature is 6T, average of field measurements (acres)
A a arca of isotherm whose excess temperature-is 6T, m
maximum of field measurements (acres)
AT = excess temperature and l6T, = discharge excess temperature.
- Equations 46 and 47 were determined for values of $T/6To between approximately 0.17 and 0.37. - This corresponds to temperature- ,
excesses from approximately 3 to-70F for a discharge excess temperature of 20 0F.
O 1.4-30
The conditions existing during the field measurements were O
equivalent,for a dischstge excess temperature of 200 r,to a lake elevation of 248.7 feet USGS and a lake temperature of 4 0er.
It can be assumed that the area-temperature behavior along the lake bottom follows the subsurface, six foot depth plume behavior determined in Section 1.4.1.1.4. In this manner, equations 46 and 47 will be extended to ambient conditions other than those existing during the measurements.
1 l
l Although not enough information is available to define lake '
bottom isotherm shapes, two items of interest were noted.
Firstly, the extent of the isotherms will range from approximately 700 feet for the 70r isotherm to approximately 1000 feet for the 30F isotherm. Secondly, the maximum widths of the isotherms occur at approximately 0.75 of the total distance along the centerline.
1.4.2.3 velocitv Decay The decay of velocity along the path of the plume can be estimated from the temperature decay. In the near field, plume temperatures are decreased chiefly by mixing with the cooler ambient water.
Some heat is also lost to the atmosphere, but, as shown in Section 1.4.1.1.2.1, this contribution is small. The decrease in plume velocity arises,as does the decrease in temperature, chiefly from &
mixing with the lower momentum ambient water. Therefore, it T can be postulated that, in the near field, the dimensionless velocity decays in the same way as the dimensionless temperature.I14)
This can be expressed as, U =0 (48)
U n 6T o where U = plume excess velocity and Do = discharge velocity.
Given the temperature decay and the discharge velocity, it is therefore possible to calculate the velocity at any point in the plume. Figure 1.4-27 shows the discharge velocity, which depends only on the lake elevation, for the range of conditions encountered at the site, 1.4.2.3.1 Exposure Time The use of equation 48 in conjunction with the temperature decay determined in Section 1.4.1.1.4 allows determination of the time it takes for a parcel of water to cool to a given temperature.
If this calculation is performed along the plume's surface centerline during still water conditions, maximum exposure times O
1.4-31
'l O result. The relationship between time, distance, and velocity is, t a dt = b ds, (4 9)
U t
o o where t o = travel time from condenser entry to lake discharge t = travel time from condenser entry to a a = distance along path of plume measured from lake discharge.
If equation 48 is substituted into 49, the result is, 8
dT ds t=to+ g j{- (50) o where 6T is a function of s. Note tNit. AT at the centerline is gival g-, in Table 1.4-5.
(_) 1.4.2.3.2 Plume Trajectory It is explained in Section 1.4.1.1.2.1 that the effect of the ambient currents, for the normally occurring current range at Ginna, is a gradual bending of the plume's trLjectory. Since the model described in Section 1.4.1.1 is derived in terms of center-line distances along the path of the plume, the temperature distri-bution in the presence of an ambient current can be estimated from knowledge of the plume's trajectory.
The absolute velocity along the conterline of plume is the resultant of the plume and ambient velocity ecmponentr,. For an ambient velocity perpendicular to the discharge velocity, this leads to the expressions, C
sin 6 = - (51)
U2+U 2
. c a and cos 0= (52)
U*c O
1.4-32
where U
11e = plume centerline excess velocity
=
h 6
n = ambient velocity angic between the ambient velocity component and 2 2 the resultant velocity and Og = resultant velocity.
c If xis taken as the direction of the discharge and y as the direction of the ambient current, then dx
= sin 0 (53) ds and dy
= cos 6 (54) ds Substituting equations El and 52 into 53 and 54, respectively, and integrating both sides yields, -
s x- = c ds (55)
U o c s
and y ^
= ds , (56) 2 2 o
1 fUe4g a where x,y , and s are measured from the center of the discharge plane. ::ote that U c can be calculated as a function of s by use of equation 48 and the information in Table 1.4-5.
1.'4.2.4 Winter Pecirculation When intake temperatures drop below 40 F, such as occurs during the winter, discharge water is recirculated so that the condenser inlet water temperature is 400F, This has the effect of lowering the flow rate of the discharge to the lake while raising the discharge excess tenperature. Figure 1.4-28 shows the discharge flow rate and excess temperature as a function of ambient (intake) temperature.
Although the model developed in Section 1.4.1.1 is not directly applicable to ambient temperatures much below 400F, it cr.n be used as an indicator of the size of the winter plume. This is because O
1.4-33
_ ._ ~ . _ . _ _ _ . _ _ . . - - . - -
i I
() the basic mechanisms which govern plume dilution are similar whether the plume is buoyant or not. That is, dilution is governed by the mixing properties of the plume with the ambient.
The major differences between the buoyant and non-buoyant cases are the buoyant plume will lose heat to the atmosphere while the l
non-buoyant plume will exhibit more complete vertical mixing. !
As shown in section 1.4.1.1.2.1, the former difference is unimportant. The latter difference will cause a deepening of the thermal ficid. However, the increased vertical mixing will also result in more rapid decay of the discharge temperatures.
In the sections which follow, plume areas along the surface and six foot depth are presented for the winter season. The calculations are based on the model of Section 1.4.1.1 and are intended only as general guides to the overall extent of the thermal field. They are, accordingly, indicated as dashed lines in the appropriate figures. Volumes have also been calculated.
These are shown as solid lines in order to demonstrcte that, although the vertical trajectory of the winter plume makes the surface and six foot depth areas only general indications of plume extent, the volumes, or overall plume size, will be better approximations.
O
() -
1.4-34
1.4.2.5 Seasonal Thermal Ef fects O
Thermal ef fects of the Ginna discharge during normal (expected) and extrene (vorst case) seasonal conditions follow. Figures describing the seasonal thermal effects are arranged by type rather than season. Figures 1.4-29 through 40 illustrate surface and six foot depth isotherm maps for the seasonal cases. Figures 1.4-41 through 44 give the corresponding isotherm areas, while Figure 1.4-45 relates lake bottom isotherm areas. Figure 1.4-46 shows isotherm volumes, 1.4-47 through 52 gives exposure times, and 1.4-53 through 58 illustrates plume trajectories.
All plume calculations assume a vertically uniform ambient temperature. If the ambient temperatures are not vertically uniform, such as occurs in the summer, the plant will take in colder water than will be seen by the discharge. This means that the discharge excess temperature will be decreased by the amount of stratification between the intake and discharge icvels. This will reduce the thermal effects of the discharge for two reasons.
First, the lower discharge excess tenperature means lower excess temperatures throughout the plume's development.
Second, the lower discharge excess temperature lowers the buoyancy of the plume, thus resulting in greater discharge -
diluting capabilities. Neglect of ambient stratification, there-fore, results in conservatively large summer plume predictions.
1.4.2.5.1 Expected Seasonal Conditions Expected seasonal conditions, given in Table 1.4-8, are defined as the expected plume under average ambient conditions.
1.4.2.5.1.1 Expected Winter Plume As explained in Section 1.4.2.4, the mathematical model was not derived for winter conditions. Because of the uncertainty in plume configuration, no isotherm maps were drawn. Figures 1,4-41 and 42 show surface and six foot depth areas calculated, from the model. These areas are presented to give a general idea as to plume extent and are indicated as dashed lines, as described in Section 1.4.2.4. Figure 1.4-46 gives the expected winter volumes, as calculated from the model. As noted in Section 1.4.2.4,these values are larger than those which will occur, due to the increased vertical mixing caused by the decreased buoyancy effects.
1.4.2.5.1.2 Expected Spring Plume Figures 1.4-29 and 30 show the expected surface and six foot depth isotherms. Figures 1.4-41 and 42 give the corresponding areas. Figure 1.4-45 gives the area along the lake bottom, 1.4-35
d while volumes can be found from Figure 1.4-46. The 3 F isotherm has areas on the surface, six foot depth and bottom of 86, 32, and 5.6 acres, with a volume of 460 acre-feet. Figure 1.4-47 shows that the maximum time a parcel of water will be at 30 F or higher is 42 minutes.
Figure 1.4-53_shows the plume trajectory for alongshore currents of 0.17, 0.33, and 0.50 fps. Note that these trajectories do not take into account the presence of Smoky Point. Alongshore ambient currents will be deflected into the body of the lake due to the existence of Snoky Point. This phenomenon is not accounted for here. The trajectory curves assume an undeficcted ambient current direction.
1.4.2.5.1.3 Expected Summer Plume Pfgures1.4-31and32showthesurfaceandsixfootdepthisotherms.
3 F areas along the surface,'six foot depth, and botten, as fcund in Figures 1.4-41, 42, and 45, are 87, 27, and 4.6 acres, respec-C tively. The 3 F volume, as found in Figure 1.4-46, is 420 acre-feet. The 3,F exposure time, found in Figure 1.4-48, is 39 minutes. Figure 1.4-54 shows the plume trajectories for currents up to 0.5 fps. As noted in Section 1.4.2.5, these thermal effects ,
are conservatively large in that ambient vertical temperature
{} stratification is not considered.
1.4.2.5.1.4 Expected Fall Plume Table 1.4-8 shows the expected fall lake elevation to be over one foot lower than the spring and summer elevations. The re-sulting larger discharge velocity, in cenjunction with the low ambient temperature, can be expected to cause a decrease in the plume size. This decrease should be most pronounced at the surface,
' as the increase in Froude number will increase plume mixing.
Subsurface areas, however, will also be sffected by the decrease in buoyant plume rise.
Egpected fall isotherms can be found on Figures 1.4-33 and 34.
3 F areas, found on the same figures as the other expected
' stasonal conditions, are 63, 30, and 5.1 acres, corresponding tg the surface, six foot depth,Note and that, bottem, respectively. The 3 F volume is 380 acre-fect. as expected, the overall :
plume size has decreased from the spring and summer, although the subsurface areas have not.
The maximum 3 F exposure-time is 30 minutes, as seen in Figure 1.4-49. Figure 1.4-55 shows the plume trajectories.
(:)
1.4-36
= ._ - __ _ _- _ _._ _ , _ _ _ _ _ . _ _ - . - . _ . _ _ _ _ . _
1.4.2.5.2 Extreme Seasonal conditions Extreme seasonal conditions were defined as high lake elevations and high lake temperatures, both conditions being conducive to low rates of plume thernal decay. For the winter, when discharge-intake recirculation occurs, the lowest ambient temperature results in the largest thermal field due to the increase in excess temperature and decrease in diceharge velocity. Seasonal extreme elevations and temperatures were taken as the daily extreme found in the entire record described in Section 1.4.2.1.
These ambient conditions were combined with the " worst case" plume predictions described in Section 1.4.1.1.5.2 and the maxi-mum bottom areas described in Section 1.4.2.2. The result can be considered an upper limit to the size of the Ginna plume.
It should be noted that most plumes will exhibit behavior cimilar to the expected plumes, with the frequency of occurrence sharply decreasing as extreme plume behavior is approached. Table 1.4-8 shows the extreme seasonal conditions.
1.4.2.5.2.1 Extreme Winter Plume As explained in Section 1.4.2.4, the mathematical model was derived for buoyant plume behavior. During the winter, the negative buoyancy of the plume makes its configuration uncertain.
Figures 1.4-43, 44 and 46 show the surface and six foot depth isothermal areas along with the volumes. As noted in Section g,
1.4.2.4, these values are conservatively large.
1.4.2.5.2.2 Extreme Spring Plume Figures 1.4-35 and 36 show the surface and six foot depth isotherm maps. Figures 1.4-43 and 44 give the corresponding areas for each season. Figures 1.4-45 and 46 give the seasonal lake bottom areas and volumes, respectively, for all geasonal conditions.
The surface, six foot depth, and bogtom 3 F areas are 463, 133 and 9.5 acres 6 respectively. The 3 F volume is 2100 acre-feet.
The maximum 3 F exposure time, shown in Figure 1.4-50, is 155 minutes. Plume trajectories are given in Figure 1,4-56.
1.4.2.5.2.3 Extreme Summer Plume Figures 1.4-37 and 30 shog the extreme summer plant induced thermal distributions. 3 F areas are 396, 119, and 8.5 acres, fgr the surface, sixfootdepth,andbottom,respectfvely.
Figure 1.4-51 gives the 3 F The exposure 3 F volume is 1800 acres.
time as 126 minutes. Figure 1.4-57 gives plume trajectories.
As noted in Section 1.4.2.5, these thermal effects do not account for vertical temperature stratification in the ambient.
Consideration of this phenomenon would lower the predicted effects of the summer plume. g 1.4-37
l.4.2.5.2.4 Extreme rail Plume i
As in the case of the expected conditions, extreme fall con-ditions have lake elevations much less, more than two feet O less in this case, than the extreme spring and summer con-ditions. In addition, the extreme fall lake tcmperature is much less than that of the extreme spring and surrer. The result will be a decregse in plume si:c, chiefly reflected in near surface areas. 3 r surface, six foot depth, and bgtton areas are 257, 111, and 7.9 geres, respectively. The 3 r volume is 1400 acres. The 3 I exposure time, as found from rigure 1.4-52 is 84 minutes, reflecting the relatively large discharge velocity and the rapid temperature decay. Extreme fall plume trajectories are given in rigure 1.4-58.
1.4.2.6 parametric Thermal Plume Analysis As shown in Section 1.4.1.1, of the factors which might affect the Ginna plume, only variations in lake elevations and temperatures will cause major variations in the size of the discharge plume. As the lake elevation increases, the discharge velocity decreases. This results in a decrease of the mixing capabilities of the plume. As the lake temperature increases, the nonlinear temperature-density relationship of water causes an increase in plume buoyancy. This behavior inhibits plume mixing and causes the plume to spread on the lake surface.
Surf ace and six foot depth isothermal areas were calculated for lake elevatiops cf 244 to 250 feet USGS and lake temperagures O of 40 through 80*r. Results for lake temperatures below 40 r, which include discharge-intake recirculation effects, are also shown for completeness. As indicated in Secticn 1.4.2.4, areas for ambient temperatures less than 40 F should be interpreted as indications of overall plume si:e. These areas are also useful in determining isothermal volumes, which will give a better, but still conservatively large, idea of the overall plume size for lake temperatures less than 40"F. It is of interst to note that surface isotherm areas decrease with decreasino lake temperature. However, belcw 40 0 r, surface isotherm' areas will increase with decreasing lake temperatures due to winter recircu-lation (see Section 1.4.2.4) . ' This behavior is noted on the figures discussed below, rigures 1. 4-59 through 62 show expected 2,3,5 and 10 F surf ace areas. For the range of conditions considered, other than winter, these values range from 56 to 225 acres, 41 to 167 acres, 24 to 97 acres, and 6.7 to 27 acres, respectively. As explained above, the isothermal areas increase with increasing lake temperatures and elgvations. Figures 1.4-63 through 66 show expected 2,3,5 and 10 r six foot depth areas. For the non-winter conditicns, these areas range frem 31 to 57 acres, 22 to 40 acres, 12 to 20 acres, and 2.7 to 4.0 acres, respectively. Six foot depth areas increase with increasing lake elevation but decrease with in-creasing lake temperature. The former shows the effect of the 1.4-38
O decreased mixing caused by the decrease in discharge velocity.
The latter is caused by an increase in plume buoyancy, causing the plume to rise from the six foot level earlier in its development. This increate in buoyant rise causes an increase in surface areas but a decrease in subsurface areas.
Figures 1.4-67 through 69 show isothermal arcag along the lake bottomforlaketemperaturesbetween40andg0Fandlake elevations between 244 and 250 feet USGS. 3 r expected bottom areas range from 3.8 to 6.9 acres. The behavior of the lake bottom isotherms with varying temperatures and elevations is the same as the behavior of the six foot depth isotherms.
Figures 1.4-70 through 73 show worst case 2,3,5, and 10 F excess temperature areas along the surface. For the same range of lake elevations and lake temperetures considered for the expected plume discussion, these areas range, in acres, from 150 to 606, 116 to 471, 74 to 298, and 25 to 100, respectively.
Six foot depth areas, shown in Figures 1.4-74 through 77, range from 100 to 216 acres, 75to159 acres,f5to90 acres, and 13 to 23 acres, respectively. Maximum 3 P lake bottom areas range from 5.4 to 11.3 acres.
Parametric isothermal volumes can be estimated from the surface a and six foot depth isothermal area information. !!ote that lake W.
bottom areas are always much less than six foot depth areas.
Using the trapezoidal integration rule and assuming zero areas at 10 foot depth yields, V= 3A0 + SA6 (57) where V e volun.e (acre-feet)
A0= surface area (acres) and A6= six f t depth area (acres!.
The use of equation 57 gives approximate 3 P expected volumes from 260 to 630 acre-feet for lake temperatu5es fr m 4 t 8 F and elevations from 244 to 250 feet USGS. 3 F worst case volumes range from 760 to 2000 acre-feet.
The centerline time-temperature decay of expected and worst case plumes were calculated for lake elevations of 244 through 250 feet USGS. As shown in Table 1.4-5, the surface centerline temperature decay is independent of Froude number, and, therefore, ambient temperature. Since it was assumed that the excess velocity decays in the same way as excess temperature, the 1.4-39
O calculated centerline surface exposure times are independent ofangient. temperature. As shown in rigures 1.4-78 through 81, 3 P exposure times range from 21 to 76 minutes for the expected plume and 40 to 149 minutes for the worst case plume.
The larger elevations result in longer exposure times because the discharge velocities are lower.
O I
i l
l l
LO 1.4-40
. _ . _ . _ . , _ . . - ~ - _
1.4.3 PliYSICAL ErPECTS Or DISCL 1.4.3.1 Velocity Effects 1.4.3.1.1 Surface Velocities As explained in Section 1.4.2.3, plume surface velocities can be assumed to decay in the same manner as plume surface tempe5atures. Discharge execas temperature has been taken as 20 r for all conditions except lake temperatures less e
than 40 F. Discharge velocity, on the other hand, varies with lake elevation, as shown in Figure 1.4-27.
Table 1.4-9 shows the surface excess velecity decay for seasonal conditions, as a function of distance along the plume trajectory. It is of interest to note that higher discharge velocition result in greater mixing of the discharge and ambient cooling water. This results in a greater velocity decay rate. Expected seasonal conditions show excess velocities of the same magnitude as the lake approximately 4000 feet from the discharge. This distance is approximately 8000 to 9000 feet for the extreme conditions.
1.4.3.1.2 Bottom velocities In May 1974, RG&E sponsored 3 field surveys to determino discharge induced lake bottom temperatures and velocities at the Ginna site. (See section 1.4.2.2 for a discussion of bottom temperatures. ) Velocities and areas were reduced to dimensionless form and the relationship betwoon them determined.
The result was, A, =
-20.84h-+9.20, .36>U/Un >.18 (58) o and A m
= -39.62 UU +17.30, .36>U/Ug >.18 (59) where U = bottom velocity Ug = discharge velocity A, = area of isopleth of velocity U, average of field measurements (acres) and A*
= area of isopleth of velocity U, maximum of field measurements (acres).
O 1.4-41
The areas determined f rom equations 58 and 59 were applied to conditions other than +. hose existing during the field measure-monts by multiplying oy appropriate scale factor ratios, rigure 1.4-82 shows average and maximum lahe bcttom scour areas, defined as areas along the lake bottom where the velocity is greater than 1 fps, for lake clovations from 244 to 250 feet USGS. Average scour areas range from 0.4 to 2.8 acres; maxi-mum areas range from 0.5 to 5.2 acros. Spring, summer, and fall expected seasonal conditions correspend to average areas of 2.6, 2.6 and 2.8 acres, respectively. The higher area for fall reficcts the lower lake elevation. Spring, summer, and fall extreme seasonal conditions correspond to maximum areas of 0.1, 2.4, and 4.7 acres, respectively. The low value for spring results from the high lake elevation, 250.19 feet USGS.
1.4.3.2 Concentrations It is possible to determine the characteristics of chemical dilution in the Ginna discharge by drawing the analogy between temperature and chemical dilution. Both are chiefly products of mixing of discharge and ambient water. Temperature decay also occurs by atmospheric cooling but, as shown in Section 1.4.1.1.2.1, this is unimportant in the near field.
The characteristics (isopleth shape, area, and volume) of the chemical dilution will be the same as the characteristics of the thermal dilution if the dimensionless excess concentration O is equal to the dimensionless excess temperature. That is, C -C * = AT
' (60)
Co-C a ATo where C = concentration C,= ambient concentration C = discharge concentration o
6T = excess temperature and 6T o
= discharge excess temperature.
Equation 60 can be used to relate concentration characteristics with the thermal characteristics developed in Section 1.4.2.
If ecuation 60 is satisfied, then the isopleth of concentration C will have the same shape, area, and volume as the isotherm of excess temperature 6T .
O 1.4-42
llh 1.4.3.3 Shoreline Erosion The major erosion effect of the Ginna discharge is bottom scouring in the vicinity of the discharge. This has been discussed in Section 1.4.3.1.2, where it was shown that scoured areas may range from 0.4 to 5.2 acres, depending on lake and discharge conditions. It should be noted that the scour areas exhibit shapes similar to isotherm shapes, their major influence being directed offshore.
It is also possible to postulate that a shoreline discharge of water, such as exists at Ginna, can act as a barrier to movement of lake sediments. If tne discharge were to give the same effects as a solid barrier, depositien would occur upstream of the discharge and erosion would occur downstrean of the discharge. However, a number of factors mitigate this behavior.
Currents at the site are alternately in both alongshore directions with a predominance of west to east currents. This would cause alternate erosion and deposition on either side of the discharge, with a small net effect. Furthermore, the plume completely blocks the normal alongshore flow for a distance of approximately 1000 feet offshore. After this point, the along-shore flow can pass under the plume. lll No shoreline erosion due to discharge operation has been noticed since Ginna began operating in 1969.
O 1.4-43
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