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Heat Source Model User Guide - Department of Environmental Quality

1. Meander 4 Width 5 6 3 ENTRENCHMENT RATIO fo Bankfull l Width Entrenchment ratio refers to the vertical containment of the channel Itis quantified as the flood prone width to bankfull width ratio Entrenchment Ratio Entrenchment Ratio Flood Prone Width Entrenchment Ratio Bankfull Width 5 5 a m i i Bankfuli ip Width Page 157 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 5 7 DIGITIZING A STREAM LAYER Conceptually what you need to do to create a stream layer from the aerial imagery by tracing the stream Following are the steps that need to be completed 1 Add an existing 1 100 000 or 1 24 000 stream coverage to your view 2 Add the appropriate aerial imagery to your view Now you have a view containing the aerial imagery and coarse stream coverage The coarse stream coverage will help guide you during digitization in case you lose track of the stream and or its tributaries You may be required to re project the coarse stream coverage in order to match the aerial imagery projection Now you are ready to begin creating your 1 5 000 digitized stream layer 1 Zoom into 1 5 000 or closer if the aerial imagery resolution is sufficient 2 Goto View New Theme 3 Inthe Feature Type dialog box select Line 4 Give your theme a name and save it 5 Go into the Legend Editor for
2. eae a ee V za E e 4 3 F Eo ji t FIGURE 3 12 Hyporheic flows through stream bar substrate Squaw Creek Oregon ND ia FIGURE 3 13 Vertical Hyporheic Surface and Flows Exchanging DSi subsurface Channel Bottom Qs parameters used to s calculate hyporheic exchange Porosity P Hydraulic Conductivity Ks Embeddedness E Page 95 Chapter IIl Dynamic Mass Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Darcy s Law is used to calculate the seepage flow exchange with water column flows as a function of hydraulic head seepage cross sectional area and hydraulic conductivity It is assumed that hyporheic flows are conserved volume is not lost from the water column or saturated streambed via this process This assumption allows that hyporheic flow additions at the downstream boundary of a stream segment are accompanied by equal water column additions at the upstream boundary The cross sectional area of the seepage face As is the product of the seepage face thickness hs and the wetted perimeter Pw of the channel The hydraulic head is calculated as a function of streambed slope friction slope and stream depth Darcy s Law for Calculating for Hyporheic Flow Domenico and Schwartz 1990 dh Qhyp As Ke Fa 3 33 Change in hydraulic head per unit distance dhp hp Moist rr ae Cross Sectional Area of the Seepage F
3. Purpose select Associate WD with Rosgen Level Types to automatically assign a ASO to listed level Rosgen stream types Continuous Data Mass Transfer Data vegematic This step is not mandatory Instead WD values can be Input by the user However WSO values must be specified before bankfull morphology can be calculated You must either associate WD with Rosqgen level types or enter VD values manually before you Associate WD Bankfull Morph Evaporation Bed Conduction _ with Rosgen can calculate bankfull morphology i Levell Types Flow Routing Clear Sheets hls step is Optional Asoraonate model use and anoication are the sole responsiblity of fhe a Oregon m xm user Department of M pe OUTS Environmental s i SUING ey 7A a ie N Hide Main Menu ica e Enter Average W D as a Function of Rosgen stream Type Enter W D Data Stream Type W D A 5 B 12 C 20 E if F 20 G a Users can enter W D values to associate with Level Rosgen stream types Important e Do not spend too much time with W D or channel angle z values right now You will have the opportunity to fine turn this information once the model is completely setup e You will need to estimate the Rosgen Level stream type Chapter IV Model Operation Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 lf the letters
4. Re Exo 0 0214 05 Te 1 941 2 54 Direct Beam Solar Radiation Attenuated from Surface to Stream Bed A1 spas 1 T 2 55 Direct Beam Solar Radiation Reaching Stream Bed A2 Depp Al 2 56 Direct Beam Solar Radiation Absorbed in Stream Bed A3 A2 1 R8 2 57 Direct Beam Solar Radiation Absorbed in Stream Bed and Immediately Returned to Water Column as Heat A4 A3 0 53 1 n 2 58 Direct Beam Solar Radiation Reflected from Stream Bed A5 A2 R p 2 59 Direct Beam Solar Radiation Attenuated from Stream Bed to Surface A6 A5 1 TS 2 60 Direct Beam Solar Radiation Attenuated in Water Column Doppg A1 A4 A6 2 61 Page 48 Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Direct Beam Solar Radiation Attenuated in Stream Bed D spp7 A3 A4 2 62 DIFFUSE SOLAR RADIATION ROUTING THROUGH WATER COLUMN Transmissivity of Water for Diffuse Solar Radiation adopted from Austin and Halikas 1976 Stream Bed Reflectivity adopted from Beschta and Weathered 1984 R s Exo 0 0214 fo n 1 941 2 64 Diffuse Solar Radiation Attenuated from Surface to Stream Bed Bt saps 1 T2 2 65 Diffuse Solar Radiation Reaching Stream Bed B2 Deans B1 2 66 Diffuse Solar Radiation Absorbed in Stream Bed B3 B2 1 3 2 67 Diffuse Solar Radiation Flux Absorbed in Stream Bed and Imm
5. Zone 0 End lf Next Zone Visual Basic Code 2 40 Step 3 Direct beam solar radiation is then calculated for each of the land cover zones from the outer most zone to the inner land cover zone as a function of the shade density and the direct beam solar flux leaving the previous zone A A sppe For Zone 4 To 1 Step 1 A A 1 Yc Zone Next Zone sprg3 A Visual Basic Code 2 41 Diffuse Solar Radiation below Riparian Vegetation Position 3 Diffuse solar radiation penetrating below the land cover spgpng Is calculated as a function of the view to sky Oys and the diffuse radiation above riparian vegetation spp P srRD3 Psrp2 OvrTs 2 42 Page 43 Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Variables Measured Known Hic Land Cover Height for each Zone m VD Land Cover Density unitless Wic Land Cover Zone Width m Zic Ground Elevation Above Stream Surface for each Zone m Zone Land Cover Zone Calculated Psrg2 Direct Beam Solar Radiation below Topography gt Msap2 Diffuse Solar Radiation below Topography Dspp3 Direct Beam Solar Radiation below Land Cover a sprpz Diffuse Solar Radiation below Land Cover Ga ic Land Cover Shade Density unitless Osa Solar Altitude degrees Ovts View to Sky unitless PLic Direct Beam Path Length through
6. predicting thermal changes in impoundments EPA Water Pollution Control Research Series U S Environmental Protection Agency Washington D C Oke T R 1978 Boundary Layer Climates Maethuen and Company Ltd London England 372 pp Oregon Department of Environmental Quality 2000 Upper Grande Ronde River Subbasin Total Maximum Daily Load Park C 1993 SHADOW stream temperature management program User s Manual v 2 3 USDA Forest Service Pacific Northwest Region Parker F L and P A Krenkel 1969 Thermal pollution status of the art Rep 3 Department of Environmental and Resource Engineering Vanderbilt University Nashville TN Penman H L 1948 Natural evaporation from open water bare soil and grass Royal Society of London Proceedings Series A 193 120 145 Petersen B T Stringham and W Krueger 1999 The impact of shade on the temperature of running water Department of Rangeland Resources Oregon State University Poole G C J A Stanford S W Running and C A Frissell 2000 A linked GIS modeling approach to assessing the influences of flood plain structure on surface and ground water touting in rivers Proceedings 4 International Conference on Integrating GIS and Environmental Modeling GIS EM4 Poole G C and C H Berman 2000 Pathways of human influence on water temperature dynamics in stream channels Submitted to Environmental Management pending publication Potter M C and D C Wiggert
7. temperatures 23 7 Forested Meadow 100 O g2 75 z Direction o of Flow a z T e21 50 8 E 5 ao y Shade D 20 25 TIR Stream Temperature gt 19 l 0 OD ya N 9p LO CO O O O gt OD O O gt O O gt River Mile FIGURE 1 4 TIR derive stream temperature data and effective shade modeling indicate that 3 C stream heating corresponds to reduced shade distributions Reduced rates of stream heating are apparent in the shaded forested downstream reach Vey Meadow Grande Ronde River Oregon Terminology used to describe the observed thermal response can be complex and rather academic Terms such as cooling and heating imply a change over distance or time The temporal change in temperature should be referred to as a rate The spatial change in temperature should be referred to as a gradient For example in the meadow unshaded reach the above plot shows a 0 6 C change per river mile and 1 3 C change per hour In the forested shaded reach the above plot shows a 0 4 C change per river mile and 1 2 C change per hour By definition the meadow reach has a heating gradient and the forested reach has a cooling gradient Both reaches have rates of heating Page 17 Chapter Introduction Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 over the time period 8 00 to 16 00 however the r
8. Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Prepared by Matthew Boyd amp Brian Kasper The methods presented in this document formulate the programmed modules utilized by Heat Source and T Tools versions 7 0 These computer models are used to create spatial data sets for stream networks simulate dynamic hydraulics and thermodynamics Appropriate use and application are the sole responsibility of the user This document may be downloaded from the web site at the following URL http Awww deq state or us wq TMDLs tools htm Updated February 12 2003 amp February 20 2007 Cite this document as Boyd M and Kasper B 2003 Analytical methods for dynamic open channel heat and mass transfer Methodology for heat source model Version 7 0 Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Table of Contents CHAPTER I INTRODUCTION 1 1 Overview of Methodology 1 1 1 The State of the Science 1 1 2 Acknowledgement of Limitations 1 2 Stream Heating and Cooling Processes 1 2 1 Common Nonpoint Sources of Stream Temperature Change 1 2 2 Point Sources of Stream Warming 1 2 3 Natural Sources of Stream Warming and Cooling 1 3 Model Application Scope Scale amp Cumulative Effects 1 4 Salmonid Life Stage Thermal Ranges CHAPTER Il HEAT TRANSFER 2 1 Overview 2 2 Solar Radiati
9. Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 4 3 3 MODEL SETUP CONTINUOUS DATA Important Since continuous data are time dependent make sure that you have entered the appropriate date in the Starting Date text box located under the General Model Input tab The first time will be 12 00 AM for the starting date and incrementally increase one hour to the ending date determined by the Simulation Period Continuous data refers to ground level information measured over time such as flow rate stream temperature air temperature wind speed and relative humidity These data are used for boundary conditions heat transfer calculations and validation data Select the Continuous Data tab under the Model Setup tab in the Main Menu and then double click on the number of continuous data sites that contain any data that you intend to include as validation data or atmospheric inputs This step will format the worksheet Continuous Data which is then ready for input of these data Important Info General Model Input Model Setup Executables Diagrams e The maximum number of Data Sheets Setup Continuous Data Sheet Continuous Nodes is Purpose 100 This is a large ie list E a alerts the ath rate ee data Des number of continuous at contain either boundary conditions validation temperature Mass Transfer Data data or atmospheric data dat
10. STEPS 1 In the File drop down select Extensions 2 Check the box next to TTools 7 0 and click OK see picture below Extensions Available Extensions Toos 7 Convert Vertes to Point Cancel View T oole ViewM aker vi a a a E YPF Viewer Reset Watershed from Points I Make Default 10 DoMaticl v2 0 3 Click the TTools 7 0 menu for a drop down of the TTools sampling options Page 175 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 STEP 1 SEGMENTING THE STREAM AND CALCULATING THE ASPECT PREREQUISITES 1 5000 digitized and cleaned stream polyline theme STEPS 1 Check the Map Units under View Properties You MUST be in a projection that uses the Map Units of FEET or METERS for example OGIC has feet for Map Units while UTM has meters for Map Units Plan to stay in this projection Map Units for the remainder of using T Tools Highlight your 1 5000 stream theme in your view s table of contents select the Segment Calculate Aspect option in the TTools You will be asked to select the projection properties that you are in If you are using Ogic and Oregon Lambert is not an option you must cancel Then load the Projector OL extension and click on its button the hourglass in the view This will load Oregon Lambert projection properties i
11. where S 21 448 t jne 46 815 t joc 0 00059 t Joc 0 001813 Obliquity of the Elliptic degrees Page 31 Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Eccentricity is a parameter that specifies the shape of a conic section which is one of the standard elements used to describe an elliptic orbit position and motion of the Earth s orbit The eccentricity Ec of the Earth s orbit relative to the earth sun distance is calculated as a function of time measured in Julian centuries typ The eccentric anomaly accounts for an undisturbed elliptic motion as the angle measured at the center of the ellipse from pericenter to the point on the circumscribing auxiliary circle from which a perpendicular to the major axis would intersect the orbiting body Earth s Eccentricity of Orbit Ec 0 016708634 t jnc 0 000042037 0 0000001267 type 2 8 The angular distance of the solar sphere sun is measured eastward along the ecliptic from the dynamical equinox to the circle passing through the poles of the ecliptic and the sun The term geometric mean refers to the average geometric position which can be conceptualized as the geocentric position of an object on the celestial sohere which is the true equator and equinox but without the displacement due to planetary aberration Therefore a geometric mean of the longi
12. 1965 Canada 3 45 10 1 26 10 Brady et al 1969 South U S 2 81 10 0 14 10 Brady et al 1971 South U S 2 21 10 0 Ryan and Harleman 1973 Australia 2 83 10 1 26 10 Dunne and Leopold 1978 1 505 10 1 600 10 Bowie et al 1985 California 3 083 10 5 845 10 Wind velocity measured at a given elevation above the water surface may not be representative of the wind velocity experienced by the water body surface boundary The expressions for the wind function are specifically developed to account for this phenomenon and are highly dependent on wind speed sampling elevation above the water surface Dingman 2002 When emergent vegetation is present the attenuation of wind will be significant and since the vertical distribution of wind velocity deceases at the water surface due to frictional forces from the emergent vegetation This wind attenuation is represented as a logarithmic function Specifically the Prandtl von Karman Universal Velocity Distribution formulae for turbulent flows can effectively simulate the boundary layer wind flows experienced by the stream surface Dingman 2002 Developed by Dunne and Leopold 1978 for the Penman Method Page 62 Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Boundary Layer Wind Velocity Prandtl von Karman Universal Velocity Distribution Dingman 2002 Ws 2 Wem 2
13. CH O Ck C sed der Page 183 Methodology for the Heat Source Model Version 7 0 Wind Function Coefficient m mb s Atmospheric Elevation degrees Volumetric Weighted Thermal Diffusivity 2 Water Thermal Diffusivity 0 0000001433m s Substrate Thermal Diffusivity 0 0000045m s Surface Area of Conduction Layer m Cross Sectional Across Seepage Face m Stream Segment Surface Area m Cross Sectional Wetted Area m Wind Function Coefficient mb Bowens Ratio unitless Embeddedness Clearness Index Cloudiness 0 to 1 Muskingum Coefficients Refraction Coefficient degrees a0 Volumetric Weighted Specific Heat Capacity eG Water Specific Heat Capacity 4187 J kg C Wave Celerity 2 Substrate Specific Heat Capacity 2219 J kg C Day of Month 1 to 31 Diffuse Fraction of Solar Radiation Dispersion Coefficient Used in MacCormick Method Diffusion Coefficient Used in Muskingum Cunge Method Model Time Step s Model Distance Step m Bankfull Depth m Average Bankfull Depth m Depth of Conduction Layer m Water Column Depth m Average Water Column Depth m Solar Declination degrees 0 Slope of the Saturation Vapor v Air Temperature Curve To Emissivity of the Atmosphere unitless Evaporation Rate Eccentricity of Earth s Orbit unitless Equation of Time minutes Aerodynamic Evaporation S Symbols An
14. Direct Beam Transmissivity of Water Column unitless T Diffuse Transmissivity of Water Column unitless PLy Direct Beam Path Length through Water Column m Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 2 2 LONGWAVE THERMAL RADIATION oycwave The longwave radiation flux is comprised of a positive component atmospheric and land cover and a negative component back radiation The intensity of incoming atmospheric long wave radiation experienced by the stream surface is a function of atmospheric moisture Anderson et al 1984 Humidity and air temperature influence longwave radiation greatly while carbon dioxide and other molecules in the atmosphere have less of an influence Further Anderson et al 1984 found that the height of cloud cover affects the intensity of longwave radiation Thermal radiation emitted from surrounding land cover is largely controlled by the physical characteristics i e height and density which combine form the radiating surface area Longwave radiation emission from the surface of the stream termed back radiation is the second most important component in dissipating heat energy from the stream system Parker amp Krenkal 1969 Back radiation is best described by the Stefan Boltzmann Fourth Power Radiation Law for a blackbody as a function of the emissivity water 0 96 and water temperature McCu
15. Forest Plan To get the quad maps you want you must know either the lat long or the map names 5 7 1 CLEANING AND UNIONIZING A STREAM LAYER TTools requires that your stream layer be cleaned of all undershoots overshoots and then unionized into a single line i e merge the separate segments This section describes how to check your stream layer for overshoots undershoots and how to fix those errors 1 Make sure that you have your stream layer selected in your view 2 Select the TTools menu Page 159 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Select the Show Loose Ends option in the TTools menu Click the Show Me button to identify overshoots undershoots within your stream polyline Now your stream polyline will have all of its nodes highlighted in red or blue Blue is good and red is bad Red indicates that you have an overshoot undershoot that needs to be fixed You are only allowed to have a red dot at each terminal end of the stream polyline in your finished product s aay Page 160 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 5 7 2 CLEANING THE OVERSHOOTS Now that you have highlighted the overshoots undershoots with the Show Loose Ends tool you can o E get to
16. Ry3 So2 Rearrange to Develop the Function of Depth 2 Fidw A Rp3 S S 2 Step 2 Compute the first derivative of function of depth F dw as follows First Derivative of the Function of Depth F dw Adw F d Adw where Ady 0 005m Step 3 Calculate the new approximation for wetted depth dy Approximation for Wetted Depth dy a Ew F dw Step 4 Use the new approximation for wetted depth dy to calculate Step 1 function of depth F dw and Step 2 first derivative of the function of depth F dy Calculate the Step 3 new approximations for wetted depth dy Repeat until convergence tolerance is achieved Convergence Tolerance di dw lt 0 0001m Page 75 Chapter IIl Dynamic Mass Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Variables Measured Known n Manning s Roughness Coefficient S Stream gradient dimensionless Wee Bankfull Width m W D Bankfull width to depth ratio dimensionless Z Channel Side Slope Ratio dimensionless Calculate A Cross Sectional Wetted Area m dpe Bankfull Depth m dw Water Column Depth m dgr Average Bankfull Depth m dw Average Water Column Depth m Pw Wetted Perimeter m Q Flow Rate m Ry Hydraulic Radius m U Average Flow Velocity 2 We Bottom Width m Ww Wetted Width m 3 3 DYNAMIC HY
17. Substrate Thermal Diffusivity 0 0000045 ano Water Thermal Diffusivity 0 000000143311 Pseg Substrate Density 1600 s PH 0 Water Density 1000 lt lt K seq Sediment Thermal Conductivity 15 977 Kuo Water Thermal Conductivity 0 600 ae t Time s Calculated ac Volumetric Weighted Thermal Diffusivity Ac Surface Area of Conduction Layer m Co Volumetric Weighted Specific Heat Capacity ae dc Depth of Conduction Layer m P conduction Psp7 n Kel Pw PeL N N TeL I a Tw T Alluvium Vsed Vh o VoL Page 57 Conduction Flux Gaz Solar Flux Attenuated in Conduction Layer Porosity of the conduction layer unitless Volumetric Weighted Thermal Conductivity Ce Wetted Perimeter m Volumetric Weighted Density 4 Change in Conduction Layer Temperature from Solar Radiation C Change in Conduction Layer Temperature from Conduction C Conduction Layer Temperature C Conduction Layer Temperature Accounting for Solar Irradiance C Conduction Layer Temperature Accounting for Conduction C Water Column Temperature C Deeper Alluvium Temperature C Substrate Volume in Conduction Layer m Water Volume in Conduction Layer m Conduction Layer Volume m Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 2 4 EVAPORATION FLUX EVAPORATIO
18. US Geological Survey Department of the Interior Washington D C Atwell B H McDonald R B amp Bartolucci L A 1971 Thermal remote sensing of streams from airborne radiometric scanning Water Resources Bulletin 7 228 243 Austin R W and G Halikas 1976 The index of refraction of seawater Scripps Instit Oceanogr San Diego CA Tech Report SIO 76 1 121 pp Avery T E and Berlin G L 1992 Fundamentals of remote sensing and airphoto interpretation New York Mcmillan Bedient P B and W C Huber 1992 Hydrology and Floodplain Analysis Reading Massachusetts Addison Wesley Publishing Company Bell M C 1986 Fisheries handbook of engineering requirements and biological criteria Fish Passage Development and Evaluation Program U S Army Corps of Engineers North Pacific Division Portland Oregon 290 pp Berk A Bernstien L S and Roberson D C 1989 MODTRAN A Moderate Resolution Model for LOWTRAN 7 Tech Rep GL TR 89 0122 Geophys Lab HAFB Bedford MA Beschta R L R E Bilby G W Brown L B Holtby and T D Hofstra 1987 Stream temperature and aquatic habitat Fisheries and forestry interactions Pages 191 232 in E O Salo and T W Cundy eds Streamside management Forestry and fishery interactions University of Washington Institute of Forest Resources Seattle USA Beschta R L and J Weatherred 1984 A computer model for predicting stream temperatures resulting from the
19. fhi a a a i 1 pe ie i P EE ey Multi Spectral and thermal infrared radiometry TIR of a point source discharge and mixing zone measure the direct thermal effect Tualatin River Oregon The warm waste water discharge 22 C is located at the white arrow and is received into 17 4 C river water 19 5 Waste Water Discharge i Temperature ree 22 C 19 0 EFS 2 D 185 Mixed Temperature A z gt Increase Resulting Y RS from Dischange S Bo 18 0 Flow 1 6 C cE amp q Q vre z g 17 5 Receiving Water cs 17 5 C 17 0 7 Point of Waste i Water Discharge 16 5 CO N 00 O O T N ep LO LO LO LO LO CO Tualatin River KM from mouth FIGURE 1 6 Measured TIR data indicates a 1 6 C increase in water temperature after complete mix Tualatin River Oregon Page 20 Chapter Introduction Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 The discharge of waste water into receiving waters can affect a thermal change if the two waterbodies have different temperatures The receiving waters will change heat as a function of thermal differences and mass transfer from point sources Associated temperature changes resulting from a discharge after complete mixing with the receiving water will have a more profound thermal effect when mass transfer rates are large and the temperature of the point source
20. is different than the receiving water It is important to keep in mind that most stream and river temperatures have daily and seasonal temperature fluctuations while point source discharges tend to remain fairly constant Therefore the thermal effect of a point source on a receiving waterbody will also follow a diurnal cycle with maximum thermal effects occurring when the receiving water and stream temperatures are most dissimilar typically at night in the diurnal cycle or seasonally in winter 1 2 3 NATURAL SOURCES OF STREAM WARMING AND COOLING Stream and river temperatures are dynamic over large spatial scales regardless of anthropogenic activities and human sources of heating cooling Dynamic temperature change rates and gradients are reflective of variable background conditions And the temporal variability in natural background hydrology land cover succession and morphology combine to create a complex and somewhat dynamic background thermal condition The thermal background condition is a range instead of a static condition Natural sources that may elevate stream temperature above background conditions include scouring effects on morphology and floodplain vegetation drought fires insect damage to near stream land cover diseased near stream land cover and windthrow and blowdown in riparian areas The processes in which natural sources affect stream temperatures include increased stream surface exposure to heat transfer processes al
21. ji FIGURE 5 14 FLIP data point Ps Method Used to Associate FLIR Nearest to stream Temperatures segment data node 5 6 OTHER I TOOLS APPLICATIONS In addition to the standard suite of sampling operations TTools can be used to sample other geographic parameters One can digitize the valley edges flood prone widths bankfull widths or meander widths according to Rosgen 1996 stream channel classification protocols These widths can then be sampled with TTools and the results can be manipulated within a spreadsheet i e Excel to calculate sinuosity meander width ratio and entrenchment ratios 5 6 1 STREAM SINUOSITY Several morphology assessment methods consider stream sinuosity especially in unconfined stream reaches as an important parameter of stream health With data compiled with Tools sinuosity becomes a fairly easy parameter to quantify Stream sinuosity is the stream length to valley length ratio Sinuosity is calculated as Stream Length Stream Sinuosity Valley Length 5 3 Page 156 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 5 6 2 MEANDER WIDTH RATIO Meander width ratio is the meander width to bankfull width ratio Meander width is the belt width or amplitude of the meander geometry Meander Width Ratio Meander Width Meander Width Ratio Meander Width Ratio Bankfull Width 5 4
22. the sensitivity to bathometric data is very high facilitating the need for accurate and spatially varied channel geometry and elevation data The need for such data can create a potential problem when applying this method since it is likely that such data in the detail required is not available for most stream systems over a large spatial extent It is generally not acceptable to rely on assumed input values for data parameters in which model sensitivity is high For this reason alone it may prove difficult to apply the explicit finite difference method to large stream river systems or in stream river segments where bathometric data is limited An additional limitation to the explicit finite difference approximation is model Stability Both the Courant and frictional stability conditions must be met at all times adding several important consequences Depending on wave celerity and flow velocity computational efficiency may be reduced since the time step must change to accommodate variations in these parameters Beyond these traditional explicit method stability concerns the method is not stable when flows velocities or depths are highly variable Therefore highly managed flows withdrawals point sources etc or naturally variable flows springs large tributaries flashy flows etc become difficult to simulate using the explicit method Page 85 Chapter Ill Dynamic Mass Transfer Analytical Methods for Dynamic Open Channel Heat and Mass
23. x2 Qin Surface Inflow Rate m Qout Withdrawal Flow Rate m Qiv Inflow Rate 1 Qout Outflow Rate m QrrReB Instantaneous Flow Summation of Surface Inflows a Quwith Withdrawal Flow Rate m Vw Instantaneous Model Reach Volume m Page 98 Chapter IIl Dynamic Mass Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 3 6 CONTROLLED FLOWS AND DEPTHS Controlled flows are common where instream structures meter flow releases Obvious examples include dams weirs irrigation pushups etc It is recommended that these control flows be associated with the appropriate modeled stream reach As with controlled flows depth is often also controlled by instream structures For example a reservoir wetland or backwater depth can be entered to override the simulated condition if needed Model accuracy will be enhanced by accounting for controlled flows and or depths 3 7 7 DEWATERED CHANNELS Inherent to all of the flow routing methods presented in this Chapter is requirement that flow volumes are greater than zero Unfortunately in the western United States this some stream and river reaches are completely dewatered through diversions and withdrawals In these cases flow routing cannot be performed in the traditional manners outlined in this Chapter In terms of modeling low flows are extremely difficult to simulate recall that stream temperature c
24. 1444 1445 1654 1652 1858 GE 1959 2065 2066 2272 HB 2273 2479 HM 2480 2696 2097 2294 L No Data 9 Center your Vertex Editing cursor on a node and you will see cross hairs appear Click and hold while you move the vertex to the desired location on the channel edge 10 In order to add a node to a section of the line that needs a bend place your Vertex Editing cursor over the desired location on the line and right mouse click once 11 Repeat this process for both the right bank and the left bank until you have moved the polyline theme to the appropriate location Page 166 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Helpful Hint In some areas the channel edges may be obscured by vegetation canopy closure or the stream may be too narrow to interpret the channel edges from the aerial imagery You should leave the nodes in such locations undisturbed The result will be a bank line that is exactly on top of your digitized stream line i e you will have moved the line ONLY where the channel edges are visible in the aerial imagery When you run TTools to sample the channel widths the values recorded will be ZERO where you could not digitize the channel edge You may then modify the T Tools database manually and insert ground level measurements into the segments where the channel widths could not
25. 1991 Mechanics of Fluids Englewood Cliffs New Jersey Prentice Hall Inc Raudkivi A J 1979 Hydrology Pergamon Oxford England Rishel G B Lynch J A and E S Corbett 1982 Seasonal stream temperature changes following forest harvesting J Environ Qual 11 112 116 Rosgen D 1996 Applied River Morphology Wildland Hydrology Pagosa Springs Colorada Page 192 References Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Ryan P J and D F Harleman 1976 Transient cooling pond behavior Hydraul Eng and the Environ Proc 21 Ann Hydraul Div Specialty Conf A S C E Boseman Montana Scatterlund D R and P W Adams 1992 Wildland watershed management 2 edition John Wiley and Sons Inc Sellers W D 1965 Physical Climatology University of Chicago Press Chicago IL 2 2 pp Shanahan P 1984 Water temperature modeling a practical guide Proceedings of statormwater and water quality model users group meeting April 12 13 U S EPA 600 6 85 003 Sinokrot B A and H G Stefan 1993 Stream temperature dynamics measurement and modeling Water Resour Res 29 7 2299 2312 Stoker J J 1957 Water Waves Intersciences Press New York Torgersen C E D M Price H W Li and B A McIntosh 1995 Thermal refugia and chinook salmon habitat in Oregon Applications of airborne thermal videography Proceedings of the 15th Biennial
26. 4 Diffuse Solar Radiation above Topography gt Global Solar Flux gt Air Mass Thickness Solar Altitude degrees Radius Vector radians Air Mass Transmissivity Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 2 2 5 SOLAR RADIATION HEAT BELOW TOPOGRAPHIC FEATURES Topography In the direction from the sun to the water column the first encountered potential opaque barrier to direct beam and diffuse solar radiation is often a topographic feature If the solar altitude 8s is greater than the topographic shade angle then the stream is not shaded from direct beam solar radiation by the surrounding topography When localized topographic shading is occurs the direct beam solar radiation is assumed to be zero Regardless of whether topographic shading is occurring diffuse solar radiation is reduced in proportion to the horizon that is obscured by topography Direct Beam Solar Radiation below Topographic Features Position 2 When topographic shade is occurring Osa lt Or Dsppe 9 2 36 When topographic shade is not occurring 8g gt Or Dsppo P spe 2 37 Diffuse Solar Radiation below Topographic Features Position 2 0 OT OT 270 aa Mspp2 srp1 7 Topographic shade angle the angle between the center point of the stream and the highest topographic feature This mea
27. 6 00 PM 8 26 is 2E 8 00 PM 4 5 5 CHART HEAT FLUX The hourly simulated heat flux parameters can be plotted for any river kilometer as determined by the model distance step by double clicking on the list box These heat flux values represent water column heat transfer Chart Heat Flux Worksheet Select Stream KM to Plot Energy Balance Heat Energy Flux W m 2 Total Solar LW Air Bed Heat Rad Rad Cony Cond Evyap 8714 991200 AM _ 123 78 0 70 36 1813 1769 5298 8 14 99 2 004M 103 68 0 61 43 9 2 19 44 52 49 8 14 99 4 00AM 78 27 0 50 39 0 58 16 23 43 53 8 14 99 6 00AM 71 75 42 88 7 83 11 58 48 82 8 14 99 8 00AM 52 19 TT 34 39 16 36 11 17 61 08 8 14 99 10 004M 137 51 0 20 37 24 24 4 68 31 21 8 14 9912 00 PM 132 29 8 12 26 30 4 Sankt Eae 8 14 99 2 00PM 42 2 81 36 86 25 45 234 8 14 99 4 00 PM 10 54 j 8 79 36 11 8 47 4398 8 14 996 00PM_ 63 5 67 2594 2504 847 598 8 14 998 00 PM 84 89 388 1495 354 64 58 Series LW Rad Point 8 17 99 8 00 AM 8 14 99 10 00PM 119 23 5645 521 14 75 8274 8 15 99 12 00AM 122 4 65 61 414 21 81 74 46 8 15 99 2 00AM 98 51 5 52 1317 25 24 45 05 8 15 99 4 00AM 104 25 7246 2258 21 68 30 89 8 15 99 6 00AM 125 43 4 82 73 31 85 2202 A3 8 15 99 8 00AM 82 45 66 36 17 26 2385 28 34 8 15 99 10 00AM 99 93 32 49 08 385 1046 16 92 8 15 99 12 00PM 96 96 35 76 7 94 364 20 74 8 15 99 2 00PM 53 22 26 08 20 22 2294 43 21 8 15 99 4 00PM 4 61 2 589 347
28. DV in the TTools Data worksheet Important Info General Model Input Model Setup Executables Diagrams Run Vegematic only after all TTools data Data Sheets Associate Land Cover Physical Attributes and the physical eae pe pe f f f attribute codes data select Yegematic to assign land cover height and density are entered Mass Transfer Data Information with each land cover sample point in the TTools oe A If you missing a g Vegematic Data will also be generated for the left and right stream bank code P Associate wD lacking downstream that averages physical attribute information stop an laentily t Ie for each zone and for all zones Land cover physical attribute cell with the undefined Bankfull Morph output data can be found on the far right portion of the TTools land cover code Data worksheet Evaporation TE Make sure that the Land Cover Bed Conduction Codes and physical attribute Information is complete Flow Routing iras Clear Sheets Required for Heat Source and Shade a ET Asoraonate model use St Gi eaf and apolication are the GR Ay sole responsibility of fhe Oregon user Department of Ti POUCA Environmental ee Quality SON AN Sita is Hide Main Menu m r Land Cover Codes Worksheet Enter Land Cover Physical Height Density Overhang Land Cover Name optional Code imj n m Water 301 0 0 0 0 0 Pasture Cultivated Ag a02 Oo SU 0 0 Tre
29. Data worksheet On this worksheet there are longitudinal inputs for accretion flows and withdrawals which are handles separately from site specific at discrete locations surface and subsurface inflows Important Info General Model Input Model Setup Executables Diagrams You can always come back to add or delete Data Sheets Setup Mass Transfer Data Sheet inflow data sites Purpose without deleting the Continuous Data This step will configure Flow Data sheet based on the mass data on the transfer inputs to the stream These data will be used to Mass Transfer Data calculate hydraulics by Flow Router executable worksheet Double Chick Vegematic Associate Wi D BankFull Morph Select number of inflow data sites not including accretion flows e These data need to be in longitudinal order from upper headwaters to lower mouth longitudinal Evaporation 4 You must setup the continuous position data sheet before you can run Bed Conduct _Bed Conduction Heat Source This step is not The maximum Flow Routing necessary to run Shade a lator number of localized inflow processes Is 100 A ea Pa Required for Heat Source and Flow Router Asoraonate model use and anoication are ihe sole responsiouity of fhe Ser Environmental P OUr a BQ in E Oregon F 5 as 7 L 5 L m Tak Department of Cu DEQ INFLOW DATA SITES Inflows rates and temperat
30. Exp YPC py 0 10 Psppa Pgppa N1 Yc 0 Visual Basic Code 2 46 Variables Measured Known Hic Emergent Vegetation Height m VD Emergent Vegetation Density unitless Wic Land Cover Zone Width m Zic Ground Elevation Above Stream Surface for each Zone m Zone Land Cover Zone Calculated Doppz Direct Beam Solar Radiation below Land Cover 2a Dsap3 Diffuse Solar Radiation below Land Cover a gpp4 Direct Beam Solar Radiation above Stream Surface 7 gap4 Diffuse Solar Radiation above Stream Surface gt Osa Solar Altitude degrees PL zone Direct Beam Path Length through each Zone m SL zonge Shadow Length Cast from each Zone m Ww Stream Surface Width m Yic Emergent Vegetation Shade Density unitless Page 45 Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 2 2 SOLAR RADIATION HEAT PENETRATING THE STREAM SURFACE r j j f Diffuse Solar Al Radiation a Coke a ae L al oq erney ia g Te n e l W potaa x x Roo ntboen a f Ai Receved Radiant He i in Stream Bed A portion of solar radiation is reflected from the stream surface as a function of reflection also Known as the stream surface albedo and calculated as a function of the angle of incidence upon the surface Surface reflection of direct beam solar radiation is calculated from the solar zenith angle Osz an
31. Heat Source Model Version 7 0 Factors that Affect Stream Temperature Hydrology Flow Volume Regime Shear Velocity Point Sources Withdrawals Augmentation eHyporheic Flows Sedimentation Regardless of scale stream temperature dynamics are complicated when these three parameters i e near stream land cover channel morphology and hydrology are evaluated Many parameters exhibit considerable spatial variability For example channel width measurements can vary greatly over small stream lengths Some parameters can have a diurnal and seasonal temporal component as well as spatial variability Analytical approaches developed for stream temperature assessment that consider all of these parameters must rely on ground level GIS data and remotely sensed spatial data To understand temperature on a landscape scale is a difficult and often resource intensive task General analytical techniques employed to evaluate stream temperature are statistical and deterministic modeling of hydrologic and thermal processes Water temperature change AT is a function of the heat transfer in a discrete volume and may be described in terms of changes in heat per unit volume With this basic conceptual framework of water temperature change it is possible to discuss stream temperature change as a function of two variables heat and mass transfer Water Temperature Change as a Function of Heat Exchange per Unit Volume AHeat eT nes 1 1 w V
32. In its current form Heat Source is developed to simulate temperatures for three weeks for any period of a year The only limitation to the simulation duration is output storage Future modifications will include an output storage file that will allow longer simulation periods By design this methodology will simulate complex mass and heat transfers over very large scales at a very high resolution 1 5 000 scale Limitations to scale and resolution will largely depend on the complexity of the system and data quality It is recommended that users derive spatial data sets from high resolution and accurate GIS and remotely sensed data using the methods outlined in this document Operation of the model should include acknowledgemenis of data quality and quantity a statement of assumptions and statistical validation with measured data of simulation results Users should be reminded that methodologies for heat and mass transfer are largely physically based When model output is inaccurate it is a common practice to calibrate the model with calibration parameters By design few calibration parameters are incorporated in this methodology with the exception being the mass transfer term for evaporation rates Evaporation varies regionally and warrants user calibration a and b Page 23 Chapter Introduction Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 parameters Ho
33. NON UNIFORM HEAT ENERGY TRANSFER METHODOLOGY The rate change in stream temperature is driven by the total heat flux iotai excluding mass transfer temperature effects It is easily shown that when mass transfer is excluded a defined volume of water will attain a predictable rate change in temperature provided an accurate prediction of the heat energy flux Rate Change in Water Temperature from Heat Transfer olw A P total ot PH o Ch o Vw Ww dx Diora Pho Ch o Aw Wy dx 2 112 Ph o Ch o Ow The advective movement of water is a function of the flow velocity U Advection redistributes heat energy in the positive longitudinal direction No heat energy is lost or gained by the system during advection and instead heat energy is transferred downstream as a function of flow velocity Over a any scale the rate change in temperature due to advection is expressed in the following first order partial differential equation Rate Change in Temperature from Advection T T Ste w 2 113 ot Ox Dispersion processes occur in both the upstream and downstream direction along the longitudinal axis Heat energy contained in the system is conserved throughout dispersion and similar to advection heat energy is simply moved throughout the system The rate change in temperature due to dispersion is expressed in the following second order partial differential equation Rate Change in Temperature f
34. Stream Aspect i 95 FIGURE 5 4 Stream aspect is calculated by calculating the angle between two stream nodes Page 142 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 5 3 3 CHANNEL WIDTH FROM AERIAL IMAGERY Channel width can be measured from digitized channel edge polylines At each stream segment node T Tools measures the distance between the left and right channel edge polylines in the transverse direction i e perpendicular to the aspect Channel morphology is largely a function of high flow volume magnitude frequency stream gradient sediment supply and transportation stream bed and bank materials and stream bank stability Rosgen 1996 and Leopold et al 1964 The predominant thermodynamic influence of channel morphology is quite simple Wider channels result in the combined effect of increased solar radiation loading via decreased stream surface shade and increased stream surface area exposed to solar radiation loading A wider stream has a larger surface and a corresponding decrease in depth more water is exposed to surface heat transfer processes Stream hydraulics are a function of wetted perimeter bathymetry gradient and channel roughness Surface and groundwater interactions may change with channel morphology modifications relations to alluvial aquifer groundwater inflow hyporheic flows etc Figure 5 6 d
35. Transfer Methodology for the Heat Source Model Version 7 0 Table 3 1 Summary of Muskingum Cunge and Explicit Finite Difference Methods Muskingum Cunge Governing Continuity Equation Equations Kinematic Wave Equation Bathometric Data Moderate Requirements Computational Efficient Efficiency Stability Highly Stable Requirements Varied Flow Limitations None Provided that Q gt 0 Assumptions Wedge storage is accurately represented Travel time is accurately represented Manning s calculations are appropriate over any given time and distance step Common Watershed Scaled Modeling Applications Stream Network Modeling Page 86 Explicit Finite Difference Continuity Equation Conservation of Momentum Equation Very High Low to Moderately Efficient Variable time step is required for model stability Moderately Stable Courant Stability Condition Friction Stability Condition Unstable with Variable Flows Severely Limited Flows velocity and depths must vary gradually Vertical acceleration is negligible when compared to total acceleration Boundary friction is accurately represented Manning s calculations are appropriate over any given time and distance step Tributary flows or withdrawals do not significantly change instream flows Flows are not highly managed Manning s calculations are appropriate over any given time and distance step River Reach Modeling Floo
36. Widths 177 Step 3 Measuring Stream Elevation and Gradient 177 Step 4 Measuring Topographic Shade 178 Step 5 Sampling the Riparian Land Cover 179 Step 6 Sample FLIR Data 181 Symbols 183 References 189 Page iil Table of Contents Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Chapter Introduction Statement of Purpose Acknowledgement of Limitations and Overview of Heat and Mass Transfer Varied landscapes complex morphology and multiple land uses are common challenges in water temperature analysis Nehalem River Oregon 1 1 OVERVIEW OF METHODOLOGY This document is intended to serve as a reference for the stream heat and mass transfer analytical methodology Heat Source Chapters that follow describe in detail the mathematics and solution techniques suited for heat and mass transfer quantification Simulation of water temperature and flow dynamics over various scales i e reach watershed to basin scales is made possible with high resolution spatially continuous data coupled with deterministic modeling of hydrologic and landscape processes These processes are often interrelated and occur simultaneously and can amplify or mask the effect of other processes The methods presented in this paper are predicated foremost on data accuracy and resolution and then analytical methodology robustness Heat Source model is comprised of modules that can simula
37. Workshop on Color Photography and Videography in Resource Assessment Terre Haute Indiana May 1995 American Society for Photogrammetry and Remote Sensing Torgersen C E D M Price H W Li and B A McIntosh 1999 Multiscale thermal refugia and stream habitat associations of chinook salmon in northeastern Oregon Ecological Applications 9 301 319 Torgersen C E R Faux B A Mcintosh N Poage and D J Norton 2001 Airborne thermal remote sensing for water temperature assessment in rivers and streams Remote Sensing of Environment 76 3 386 398 United States Government Printing Office 1998 The Astronomical Almanac for the Year 1998 Washington DC Navy Dept Naval Observatory Nautical Almanac Office Watershed Sciences LLC 1999 Remote sensing survey of the Grande Ronde River Basin thermal infrared and color videography Prepared for ODEQ Corvallis Oregon 24 pp Wen Yao L R T Field R G Gantt R G and V Klemas 1987 Measurement of the Surface Emissivity of Turbid Waters Remote Sensing of the Enviornment 21 97 109 Wunderlich T E 1972 Heat and mass transfer between a water surface and the atmosphere Water Resources Research Laboratory Tennessee Valley Authority Report No 14 Norris Tennessee Pp 4 20 Page 193 References The methods presented in this document formulate the programmed modules utilized by Heat Source and TTools versions 7 0 These computer models are used to create spatial d
38. and west relative to the stream segment node In each direction east south and west TTools steps away from the stream sampling the DEM pixels for elevation and calculating topographic shade angle TTools records the value and the X and Y coordinates of the point that represents maximum topographic shade angle While this description is fairly simple the methodology is actually quite complex The overriding intent of topographic shade calculation focuses on locating the local maximum associated with each data node in the three direction East West and South Generally there are near field stream bank valley morphology etc and far field hills mountains etc topographic features that combine to form topographic shade In terms of the local effect of topographic shade only the highest directional topographic angle and not necessarily the highest topographic feature is a controlling factor With this background it becomes apparent that the search regime for the maximum topographic feature must include both the near and far field A near field search must be high resolution because the distance from the stream is small increasing the importance of even small elevation differences from stream banks and morphology The near field search directionally samples each DEM pixel for a total of twenty five pixels The highest near field 19 For a 10 meter DEM the near field search distance is 250 meters 820 feet For a 30 meter DEM the
39. be used as a calibration 3420 196 072 parameter or leave these values blank and 3250 1 98 0 32 select Calculate Muskingum Storage 3420 1 98 o2 Factor X from the Flow Router tab in the 0 780 1 98 0 2 Main Menu Important If you do not understand the Muskingum Storage X Factor select the option so to calculate the appropriate values for more information see Section 3 3 2 Muskingum Cunge Approximation SUBSTRATE INFORMATION HYDRAULIC CONDUCTIVITY BED PARTICLE SIZE AND PERCENT EMBEDDEDNESS Heat energy conduction between the alluvium and the water column and hyporheic flow methodologies utilize substrate data Hydraulic conductivity can be estimated from the dominant bed particle size silt sand gravel cobble and boulder Embeddedness refers to the ratio of fine sediment occupying the interstitial spaces in the alluvium Input of these data is very straightforward however derivations of data values can become complex and should draw from advanced morphology classifications and or measured instream data In the state of Oregon many stream networks have been surveyed for aquatic habitats and substrate measurements have been summarized in GIS databases Important In the state of Oregon many stream networks have been surveyed for aquatic habitat and substrate measurements have been summarized in GIS databases use this link to check GIS habitat survey availability htto oregonstate edu Dept ODFW freshwater inventory h
40. changes in the number of inflow sites then you may want to delete all of the data and reenter this information Heat Source Inflow Data Setup i x x Do you want to clear existing data From the Inflow Data sheet Page 109 Chapter IV Model Operation Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Flow Data Worksheet El Maurosef bevel Lostine Jan 22 olf x Epe Gi Yem et Pomat jie ete indo iHe f F x Dekan BAS 2 Get aec A A aoe e Be ri BYU Ea ex AA wie me Ae La ti 7 ail ach EA ii a P i Simulation Information z ajf Imaan Nene Lonini River a Dao DIONE al Time Step d7 mint 7 Ef Dietamnce Sto dai T0 5 Enmen Langit Ave ATAA 7 Lengiwdiun Serpe Aiie ir F0 a Thavorn Sial Hoke iri TA al a i Intiow Stes 24 1 Male Only enter Ewas Date Same F 11 data in WHITE Piast Inti Cotter flay 2 EF calls Time Zar Paci 13 NR OIE eseese TET ES Veal oto aoa a e e er eooo ea S oa MaN Ea aE etana a Eo l so Mass Transfer Inflow Locations at Inflow Heat a i a oon Locational e Hea Acenetiie so Levcanlnnal Mam Spure imio Inflow ow awy igo Information e Source Steam Acctetlon Flow Withdrawal se information Transfer Node Stream Ame Temp fete Tomp fol 3 mpm Wile km Plow fema Temp PO Flows jems ge fomlonal Proce jayiinnal km Time ems fo rg ta i 5 0 o 0 se Copper Diek i too 44 Ay pal Qrt E i DTD draa DE
41. in your view make sure that none of the features are highlighted In the Theme menu select the Convert to Grid option Name your output file IMPORTANT Do not have a space anywhere in the path to your file Do not have a space in the name of the file Underscore is OK Do not have a path to your file that is extremely long All of these issues will result in a corrupt conversion process Page 174 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 6 In Output grid extent choose same as your_veg_shapefile shp i e the extent should be same as your vegetation polygon layer 7 In Output Grid Cell Size enter 1 meter 3 28 feet THEN HIT THE ENTER KEY Failure to hit the enter key after typing in the number will not update the number of rows and number of columns fields and your conversion will crash Now click OK Under Pick field for cell values select the name of the field in your riparian vegetation polygon layer that contains your vegetation code numbers 10 Then wait a minute or two 5 10 T TOOLS OPERATION TURNING ON THE T TOOLS EXTENSION PREREQUISITES e You must have the Spatial Analyst extension TTools will not work without it e You must have a copy of TTools avx within the following folder Esri Av_gis30 Arcview Ext32 probably located on your C drive
42. is encoded on the recorded video as a means to correlate visible video images with the TIR images during post processing Data collection is timed to capture maximum daily stream temperature which typically occur between 14 00 and 18 00 hours The helicopter is flown longitudinally over the center of the stream channel with the sensors in a vertical or near vertical position In general the flight altitude is selected so that the stream channel occupies approximately 20 40 of the image frame A minimum altitude of approximately 300 meters is used both for maneuverability and for safety reasons If the stream splits into two channels that cannot be covered in the sensor s field of view the survey is conducted over the larger of the two channels 5 5 2 TIR DATA COLLECTION AND VALIDATION METHODS A calibrated FLIR radiometer is used to collect a series of digital thermal infrared images along a stream reach with the sensor maintained at a normal angle of incidence approx 90 to minimize the variability in emissivity and hence reflectivity at the water surface Sensing in the 8 12u wavelengths minimizes shortwave reflections i e the solar soectrum occurs between 0 3 to 2 2 u with a peak at 0 5 u from the water surface Wunderlich 1972 Prior to the airborne survey in stream data loggers are distributed in the basin in order to ground truth i e verify the accuracy of the TIR images Data loggers are placed evenly over the planned fli
43. m m m _ co Tig F C7 co LT F cn Time FIGURE 1 3 Solar Radiation Tub Study Effect of Shade on Water is Apparent Moore et al 1999 Page 15 Chapter Introduction Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Petersen et al 1999 closely monitored central Oregon irrigation ditches in control and shaded test conditions and found that shade overwhelmingly influenced flowing water heating rates Of particular importance was the discovery that even small increases in shade produced measurable decreases in water temperature The study also found that air temperature is a minor thermal parameter The Impact of Shade on the Temperature of Running Water B Petersen T Stringham and W Krueger Department of Rangeland Resources Oregon State University 1999 Results Shade from tarps provided a significant amount of protection from additional heating of the water at all shade levels tested affirms the importance of even small amounts of shade in moderating stream heating Conclusion At the scale of this study air temperature appears to have a minor impact on the temperature of water The dominant factor seemed to be solar radiation In the Upper Grande Ronde River remotely sensed TIR stream temperature data and effective shade comparisons mimic the results found by Moore et al 1999 and Petersen et al 1999 Lack of shade cor
44. management of streamside vegetation USDA Forest Service WSDG AD 00009 Bowie G L Mills W B Porcella D B Campbell C L Pagenkopf J R Rupp G L Johnson K M Chan P W and Gherini S A 1985 Rates Constants and Kinetics Formulations in Surface Quality Modeling 2 Edition EPA 600 3 85 040 U S Environmental Protection Agency Athens GA Bowen I S 1926 The ratio of heat loss by convection and evaporation from any water surface Physical Review Series 2 Vol 27 779 787 Boyd M and B Kasper 2002 Upper Klamath Lake Drainage Vegetation Hydrology and Morphology Oregon Department of Environmental Quality Boyd M 1996 Heat Source stream temperature prediction Master s Thesis Departments of Civil and Bioresource Engineering Oregon State University Corvallis Oregon Page 189 References Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Brady D K W L Graves and J C Geyer 1969 Surface heat exchange at power plant cooling lakes cooling water studies for Edison Electric Institute Report No 5 John Hopkins University Brett J R 1952 Temperature Tolerance in Young Pacific Salmon Genus Oncorhynchus J Fish Res Bd Can 9 6 265 323 Brown G W 1983 Chapter Ill Water Temperature Forestry and Water Quality Oregon State University Bookstore Pp 47 57 Brown G W 1970 Predicting the effects of clearcutting on stream tem
45. oO m oO O Distance River Miles FIGURE 1 5 Rates of temperature change over time and distance Vey Meadow Grande Ronde River Oregon Page 18 Chapter Introduction Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 STREAM FLOW MODIFICATIONS The simple relationship presented by Brown 1969 AT lt A2at Volume demonstrates that large volume streams are less responsive to temperature change and conversely low flow streams will exhibit greater temperature sensitivity and greater rates of stream temperature change Specifically stream flow volume will affect the wetted channel dimensions width and depth flow velocity and travel time and the thermal assimilative capacity Human related reductions in flow volume can have a significant influence on stream temperature dynamics most likely increasing diurnal variability in stream temperature Stream Flow Controls the wetted dimensior hydraulics velocity shea r stres s dispers rae Sig Te 5 J ft EO A ca i en ao Pe ae a E i ihe al J Ray Birch Creek ES Tributary to Umatiliay River Oregon Beyond the simple conception of reduced flow and corresponding reduced thermal assimilative capacity flow modifications can be highly complex in nature Diversions can reroute surface waters through irrigation systems of various efficiencies Often a portion of irrigated wate
46. of heat transfer such as solar heat and the absence of solar heat in shade A TIR image of a stratified stream reach can be interpreted to show differential heating Shade versus no shade at the stream surface However these images should not be interpreted to suggest that these differences represent short scale cooling in bulk water temperatures _Milicr Willow CE FIGURE 5 14 An Example of Thermal Stratification Identified from FLIR Image Willow Creek and Mill Creek Confluence Grande Ronde River Basin Oregon 16 40 August 25 1999 Watershed Sciences LLC 1999 Page 155 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 5 5 3 TTOOLS SAMPLING OF TIR DATA TIR grid data contain surface water temperatures that can be sampled and Statistically summarized These data are then converted to a GIS point data layer where the positional data represents the position of the sample helicopter position and the temperature data is the ten sample median of the water surface temperature The TIR point data layer offers very high resolution and needs to be associated with the stream data nodes created by TTools A procedure is available to associate TIR temperature data to stream segment data nodes where the closest TIR temperature value is associated recorded to the most proximate stream data node 8 s a a m
47. of potential imagery sources for riparian vegetation mapping aerial near infrared classified data satellite classified data etc Accuracy of the mapped riparian vegetation coverage depends upon the spatial resolution aerial extent of analysis and spectral resolution of the imagery used When mapping vegetation in narrow riparian corridors typically less than 100 meters from the stream a pixel size of one meter or smaller is desirable to maintain a high spatial resolution Regardless of the data or imagery source there are generally three steps associated with near stream land cover quantification First the land cover must be mapped remotely sensed or digitized and classified This basically involved developing polygons and populating each with a numeric code representing a near stream land cover type Second T Tools sampling of the polygon representations of land cover type at user defined intervals allows the derivation of a landscape scaled land cover type data set To this point the discussion has focused on land cover types and not the physical attributes of each type The third basic step is then to assign physical attributes height canopy density and overhang to each of the land cover types Physical attribute information can be a summary of ground level information and data measurements growth curves best professional judgment etc With this association an estimate of both land cover type and physical dimension is availab
48. partial function of near stream land cover type and condition Similarly the type of land cover that can establish grow and reproduce at any given near stream site is a partial function of the hydrologic regime the subsurface water table dynamics and the floodplain condition An obvious feedback mechanism exists between channel morphology and land cover establishment and success Human activities that change the type or condition of near stream land cover and or alter stream channels beyond what is considered channel equilibrium dimensions will likely result in altered stream surface shading patterns By definition a decrease in stream surface effective shade will have a warming effect upon water temperature Page 10 Chapter Introduction Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Examples of Two Different Land Cover and Morphology Conditions Meadow complex with high rates of summertime heating little effective shade unstable stream banks a pattern of downcutting lowered floodplain water tables and wide shallow morphology Sycan River Oregon ei E E i EA Bi i j See URN Me Nae re oe F TEn ae Oe Another meadow complex with ini summertime heating moderate effective shade stable stream banks high flood plain water table Sprague River Oregon Page 11 Chapter Introduction Analytical Methods for Dynamic Open Channel Heat and Mass Trans
49. privileges These problems can degrade the Excel files Virus protection programs can prevent VBA code from executing or can cause documented problems with saving Excel files Since the models utilize Visual Basic programming it will be helpful for users to familiarize themselves with the computer code In general the code structure relies on descriptively labeled subroutines i e SubSolarFlux With this document as a guide the code should be accessible and moderately easy to follow Important 1 To stop an executable press Ctrl Break 2 To speed simulation run times increase distance step size 3 To increase model resolution decrease distance step size 4 Be aware of the stability constraints of the models 5 Familiarize yourself with the Visual Basic code 6 Identify causes of code interruptions by inserting a code break above a the problem area and then step through the code 7 Acommon source of problems is missing data or division by zero errors 8 Submit concerns suggestions improvements and or bugs to the authors Page 123 Chapter IV Model Operation Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 4 4 1 EXECUTABLES SHADE A LATOR Shade a lator is a solar routing model that calculates the potential and received solar radiation flux at the stream surface and also provides effective shade output data Note that there is an option to a
50. recs Cover attenuated as a function of Samples canopy opening estimated with view to sky and Example of land Cover Sampling Performed by canopy density values for TTools and Used as Model Input in Heat Source each model node Direct Beam Solar Radiation below Land Cover Position 3 Step 1 Shadow Length SL c for land cover zones is a function of the sampled land cover height Hc and stream bank elevation Z for each direction and zone and the solar altitude Oc For Zone 4 To 1 Step 1 SL c Zone H Zone Zc Zone tarf Os 180 Next Zone Visual Basic Code 2 39 Step 2 If the shadow length SL c from the zone in question is greater than distance to the center of the stream then shade is occurring The path length PL over which the direct beam must travel through the land cover zone is calculated as a function of the zone width Wc and the solar altitude 6 Shade density Yc is then calculated as a function of vegetation density VD and the path length over which the direct beam must travel through the land cover zone Zone Page 42 Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 For Zone 4 To 1 Step 1 If SLi Zone gt W Zone Zone then Wc Zone Cos Oaa gt S Osx 180 PL c Zone Wo Zone 1 Exe lone PLic Zone Else PL Zone 0
51. summation of all heat energy components see Equation 2 1 Examples of heat transfer processes developed for the Grande Ronde River in ODEQ 2000 are presented in Figure 2 1 2 2 SOLAR RADIATION oar Water column solar radiation exposure rates can be simulated at a various scales stream segment to landscape scales with prediction algorithms and methods Stream surface shade production is a function of geometric relationships between the predictable nature of the sun s position and topography near stream land cover and morphology Provided an accurate location description i e latitude and longitude the exact position of the sun for any given time can be simulated as a function of time i e season and time of day Topographic land cover and or stream channel features that obstruct the sun stream vector create shade Opaque features that obstruct solar radiation such as topography and channel banks completely attenuate received direct beam and diffuse solar radiation The atmospheric air mass and land cover exhibits some level of transparency and these bodies only partially attenuate received direct beam and diffuse solar radiation Routing the direct solar beam through these partially transparent mediums results in attenuation and scattering of only portions of the direct beam and diffuse solar flux Diffuse solar radiation is received from all directions above a stream surface and will penetrate to the stream through openings in canop
52. that fail to capture the multitude of important stream parameters and processes that affect stream thermodynamics Stream temperature does not easily lend itself to simple statistical analysis For example simple regression analysis can result in spurious correlations that offer limited or poor insight into the complex thermodynamic and hydrologic processes that vary over space and time e As a general rule do not use a model to create data that can be measured It is usually cheaper to measure stream temperature via ground level and remote sensing than to derive simulated temperature data Obviously measured values i e ground level and remotes sensing are more accurate than modeled results 1 2 STREAM HEATING AND COOLING PROCESSES Parameters that affect stream temperature can be grouped as near stream land cover vegetation channel morphology and hydrology Many of these stream parameters are interrelated i e the condition of one may impact one or more of the other parameters These parameters affect stream heat transfer processes and stream mass transfer processes to varying degrees The analytical techniques employed to evaluate stream temperature can be designed to include all of the parameters that affect stream temperature provided that available data and methodologies allow accurate quantification Page 7 Chapter Introduction Page 8 Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the
53. that warrant listing e Near stream land cover plays an important role in regulating radiant heat in stream thermodynamic regimes e Channel morphology is often highly influenced by land cover type and condition by atfecting flood plain and instream roughness contributing coarse woody debris and influencing sedimentation stream substrate compositions and stream bank stability e Near stream land cover creates a thermal microclimate that generally maintains cooler air temperatures higher relative humidity and lower wind speeds along stream corridors e Riparian and instream nutrient cycles are affected by near stream land cover With the recognition that near stream land cover is an important parameter in influencing water quality the development of land cover data sets should be a high priority Variable land cover conditions require a higher resolution than most currently available GIS land cover data sources To meet this need one may need to map near stream land cover using rectified color aerial imagery Using physical attributes associated with land cover classifications sampling can be completed across a large landscape scale Summarized land cover attributes e g height density and overhang data can then be used to populate the digitized land cover polygons The high resolution of orthorectified aerial photographs allows for detailed analysis and mapping of riparian land cover within ArcView A trained technician can digitize a 6
54. that you double click on the Appropriate model use Time Inputs You and aoolcation are ihe may want to check aot sole responsiouity of fhe the worksheet input En T w P summaries to see if epar tment ae k a AE l these have been properly selected Quality ered i n E f i Hide Main Menu 4 Page 103 Chapter IV Model Operation Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 4 3 2 MODEL SETUP DATA SHEETS The next step for model setup includes developing the longitudinal input distance and model node information for the TTools Data Morphology Data and Validation Data Model nodes should match those created by TTools The distance information is the longitudinal distance from the upstream boundary condition and the stream kilometer which is the distance from the downstream boundary condition These longitudinal distances and model nodes must match those found in the TTools derived database Check the entered values for Stream Length and Longitudinal Sampling Dist if there are discrepancies Important e Do not proceed until you have confirmed Info General Model Input Model Setup Executables Diagrams Data Sheets Associate Land Cover Physical Attributes that distance Continuous Data Purpase information matches All of the executables utilize spatial data sets based on both the TTools deri
55. the center of the stream channel to derive spatial temperature patterns over the surveyed reach Derived stream temperature profiles illustrate how stream temperatures vary longitudinally along the stream course Kay et al 2001 suggests that an accuracy of 1 0 C is required to quantify stream temperature gradients identify ground and surface water inputs and create a boundary condition for basin scale hydrologic models In the Upper Grande Ronde River subbasin Oregon ODEQ found radiant measurements of stream temperatures to be accurate within 0 5 C Figure 5 12 Torgersen et al 2001 report similar levels of TIR data accuracy 30 1 1 Line S o 25 Q Ea E g 2 O FIGURE 5 12 z ee g TIR Data Validation Instream measured and 9 n 28 radiant measured stream water temperatures in E i51 e R 0 98 the Grande Ronde Basin Oregon excluding B 2 Se 0 52 C stratified areas August 19 20 1999 cc ica Significant at 0 05 10 e a a a a a a 10 15 20 25 30 Instream Measurement C Page 153 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 5 5 2 INTERPRETATION OF FLIR IMAGES What temperature does TIR data actually measure In short the answer to this question is that TIR images represent water surface or skin temperatures because water is essentially opaque to the electromagnetic spectrum greater th
56. therefore not easily quantified in a broad application such as Heat Source e Land use patterns often vary through any drainage from heavily impacted areas to areas with little human impacts However it is often difficult to find large areas without some level of either current past or upstream human impacts Few sites represent historical conditions Further some human impacts are permanent in the context of geologic time scales Attempts at simulating historical conditions cannot be validated and are likely inadequate Page 6 Chapter Introduction Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 on multiple counts Modeling applications should consider the degree of divergence between the hypothetical simulation conditions and the calibrated model condition e Uncertainties will persist since stream temperature dynamics are complex and analytical methods have limitations With this acknowledgement of limitations comes the responsibility to use your experience consult with others when needed engage in scientific reviews of your work and document limitations inherent to model output and interpretations of results Always Statistically validate model results so that others can easily recognize model performance and advise others to use your results appropriately e With recognition of inherent complexity in mass and heat transfer avoid simple analytical techniques
57. used for stream typing are not found in the listed Rosgen stream types see graphic above then a message will appear and stop the association routine The cell that contains the unrecognizable stream type leter will be identified Heat Source Rosgen Stream Typing x x Error detected in Rosgen stream type Check your values Make sure they are capital letters 4 B C E For G BANKFULL CHANNEL GEOMETRY CHANNEL SIDE SLOPE Z The next step is to input the Channel Angle z data to represent the channel side slope ratio The ultimate goal is to configure a basic trapezoidal channel dimension to match the basic channel geometry Channel profile information commonly measured when collecting instream flow data can be useful for estimating the channel side slope angle Widths t 1 z T Coordinate s ras x longitudinal a i Vi YErICal ae Z transverse Width Bottom Morphology Data Worksheet Channel Side Slope 2 Cross sectional Channel X Factor Area m Angle z 0 00 5 4 500 1 95 0 2 3 120 1 95 0 2 3 250 1 95 0 2 3 120 1 95 0 2 0 700 1 98 0 2 Page 114 Chapter IV Model Operation Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 CALCULATE BANKFULL CHANNEL DIMENSIONS With these data inputs entered the next step is to calculate the bankfull channel bottom
58. used in water quality modeling mainly stream temperature modeling TTools 7 0 is designed to assemble high resolution 1 5 000 geographic scale spatial databases This user manual is divided into three parts which discuss 1 the types of geospatial data required 2 development of the core geospatial data sets and 3 the TTools operating instructions This user manual was written under the assumption that the reader has ArcView experience Basic skills such as creating and editing themes mosaicing DEMs and obtaining and preparing aerial imagery are necessary Creating and sampling geospatial data sets requires creativity and the ability to think outside the box This user manual is not going to answer every question that will arise when preparing data for TTools sampling For example you may need to figure out how to convert a DEM from one format to another in order for ArcView to recognize it or you may obtain raw color aerial photographs that need to be scanned into the computer georeferenced and rectified before use Often times you may encounter a sub basin that has an existing vegetation layer for the upper watershed area and you will need to figure out how to incorporate that into the vegetation digitization process Once the user has the digitized stream digitized banks vegetation grid and mosaiced DEM TTools 7 0 may be used The TTools 7 0 extension contains graphical dialogs and error checks that prompt the user for input
59. using Be careful depending on the source your DEM may have elevations in feet or meters 5 When asked whether to overwrite existing data if you choose Yes all elevation and gradient data will be erased and re sampled if you choose No sampling will begin at the first zero value 6 Spatial Analyst developed by ESRI has a bug which limits the number of grid samples that it may perform Beyond which ArcView fatally crashes and reports a Segmentation Violation error TTools will prevent this disaster from happening Depending on the size of your T Tools point theme you may get a message that says Spatial Analyst has reached its sampling capacity Click OK and TTools will automatically save your project and close your ArcView session At this point re open your ArcView project and start the Measure Topographic Shade process again This time DO NOT overwrite existing values and T Tools will begin sampling where it left off last time 7 Repeat this process as many times as necessary until you see a window pop up that says Topographic Shade Angles have been calculated STEP 5 SAMPLING THE RIPARIAN LAND COVER This procedure uses Spatial Analyst to sample a grid theme Spatial Analyst can perform a limited number of commands in a given ArcView session before causing a Segmentation Violation and crashing ArcView Therefore it is strongly recommended that you save the project complete
60. work fixing the Seea e e E stream polyline Sure ae oe T Remember you will have ma Eat to click the Show Me A button each time you pan Mms or zoom in out of your view Use your magnifying glass tool to zoom in to an overshoot undershoot The image below illustrates an overshoot which was highlighted in red by the Show Loose Ends tool SO NOW YOU NEED TO MAKE SOME REPAIRS Select your stream polyline theme in your view Go to Theme Start Editing Go to Theme Properties In the pop up window select the Editing icon on the left Check both the interactive and general snapping boxes Click OK 4 Now you need to select the Line Splicing tool from your tool bar Itis in the drop down of the line drawing button and looks like this a 5 Use your cursor to draw splicing lines on each side of the overshoot as seen below ip ee ee e Fia4tte ea Segment Length UM m Length Dm Page 161 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 6 Now you can use the Select Feature tool to select each of the line segments that you don t want to appear in the end product After you have selected each one hit the delete key to get rid of it Your goal is to delete the overlapping lines and the splice lines that you just created DO NOT delete the stream polylines outside of the splice line
61. 00 foot wide riparian corridor for a 50 mile stream in about one day Ground level data must be applied to determine species composition and height values Canopy densities can be visually determined from the aerial photographs An additional benefit of using orthorectified aerial photographs is that the true color or panchromatic images allow visual decipherment of tree types and canopy densities Features such as roads and buildings are also easy to map from aerial photographs as opposed to alternative spectrum i e infrared images Aerial photograph analysis facilitates the development of dozens of riparian vegetation classes whereas most alternative spectrum satellite data can be translated into fewer and more general land cover classes The image below exemplifies some riparian classifications that were developed from black and white DOQ interpretation at a 1 5 000 scale Near stream land cover vegetation mapping can be completed on a sub basin fourth field watershed scale Large rivers streams third order and higher and selected major tributaries are typically the focus Total river miles mapped may be up to approximately 200 to 500 miles in larger sub basins Page 145 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 FIGURE 5 7 Digitized Near Stream Land Cover from a DOQ at 1 5 000 Trask River Oregon There are a number
62. 1 Select the Measure Elevation Gradient option in the TTools menu 2 Select your TTools point theme 3 Select your DEM grid theme 4 When asked to select your DEM elevation units choose the units of the values that are in the actual DEM that you are using Be careful depending on the source your DEM may have elevations in feet or meters 5 When asked whether to overwrite existing data if you choose Yes all elevation and gradient data will be erased and re sampled if you choose No sampling will begin at the first zero value 6 Spatial Analyst developed by ESRI has a bug which limits the number of grid samples that it may perform Beyond which ArcView fatally crashes and reports a Segmentation Violation error TTools will prevent this disaster from happening Depending on the size of your T Tools point theme you may get a message that says Spatial Analyst has reached its sampling capacity Click OK and TTools will automatically save your project and close your ArcView session At this point re open your ArcView project and start the measuring elevation gradient process again This time DO NOT overwrite existing values and T Tools will begin sampling where it left off last time 7 Repeat this process as many times as necessary until you see a window pop up that says Elevations and gradients have been sampled STEP 4 MEASURING TOPOGRAPHIC SHADE This procedure uses Spati
63. 28 2 110 k Zo Variables Measured Known Cho Specific Heat of Water H Humidity unitless Hic Height of Emergent Vegetation m k Wind Velocity Coefficient k 0 4 Pho Density of Water 998 2 Ta Air Temperature C Calculated a Wind Function Coefficient _ b Wind Function Coefficient Aw Stream Segment Surface Area m Br Bowens Ratio unitless A Slope of the Saturation Vapor v Air Temperature Curve ey E Evaporation Rate E Aerodynamic Evaporation x Vapor Pressure Based on e mb e Saturation Vapor Pressure Based on Ty mb D conduction p D iongwave p Qout Page 63 evaporation solar Substrate Conduction Flux a Evaporation Flux a W Longwave Radiation Flux z Solar Radiation Flux 7 Change in Stored Heat eg Water Advected Heat a Psychrometric Constant 72 Latent Heat of Vaporization a Adiabatic Atmospheric Pressure mb Flow Rate m Subsurface Inflow Rate m Surface Inflow Rate m Withdrawal Flow Rate m Subsurface Inflow Temperature C Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Calculated continued Tin Surface Inflow Temperature C Tour Withdrawal Flow Temperature Ty C Tw Water Temperature C f W Wind Function gt mb s W Wind Velocity Measured at 2 meters Above Surf
64. 3 354 34 92 8 15 99 6 00PM 31 49 57 1496 476 1529 21 35 8 15 99 8 00PM 30 42 16 34 4662 21 36 11 18 8 15 99 10 00PM 35 77 10 58 3236 1415 434 8 16 99 12 00AM 58 61 28 7 1997 043 5031 Page 130 Chapter IV Model Operation Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 4 5 6 CHART EFFECTIVE SHADE Recall that effective shade is a ratio of potential and received solar radiation heat Effective shade data is calculated at each model distance step and plotted longitudinally Stream Effective KM Date Shade 51 54 51 44 51 34 51 24 51 14 51 04 50 94 50 84 50 74 50 64 50 54 50 44 50 34 50 24 50 14 50 04 49 94 49 84 49 74 49 64 49 54 49 44 49 34 ANAA 8 15 99 8 15 99 8 15 99 8 15 99 8 15 99 8 15 99 8 15 99 8 15 99 8 15 99 8 15 99 8 15 99 8 15 99 8 15 99 8 15 99 8 15 99 8 15 99 8 15 99 8 15 99 8 15 99 8 15 99 8 15 99 8 15 99 8 15 99 niacin 0 06 0 12 0 27000001 0 19 0 36000001 0 76999998 0 18000001 0 13 0 17 0 55000001 0 64999998 0 38 0 36000001 0 11 0 1 0 22 0 23 0 12 0 2 Effective Shade Chart Shade Worksheet 100 90 80 70 60 50 40 30 20 10 0 River km 4 5 7 OTHER OUTPUT DATA WORKSHEETS OUTPUT HYDRAULICS O O O O O Oo Daily hydraulics data are listed in the Output Hydraulics worksheet The daily data that can be found on this wo
65. 34 0 55 1 57 0 29 15 30 0 32 0 56 1 52 0 17 29 90 O24 0 46 1 54 0 17 2f 20 0 26 0 52 Page 122 Chapter IV Model Operation Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 4 4 EXECUTABLES Three executables can be accessed and run independently from the Main Menu Shade a lator Flow Router and Heat Source Shade a lator is the solar routing routine from the sun to the stream surface It can be used to simulate effective shade and stream surface solar exposure Flow Router is the dynamic flow routing methodology that can be used to simulate hydraulics and wetted channel dimensions Heat Source simulates water column temperature dynamic flow routing and heat transfer processes Model inputs and outputs are unique for all three executables Model performance will vary by computer type and software installations Microsoft Excel has some issues that may create problems with the model Namely model bloat can quickly grow the file to large sizes in the course of one model run There is not an easy way to prevent this phenomenon except to manually delete worksheet cells that are not in use by the model The minimum model size is roughly 5 megabytes but a model setup and simulation may commonly approach 20 megabytes We recommend that you run Office2000 or later Sharing Excel files from a network can cause documented problems from the auto save functions and read write
66. 4 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 5 8 DIGITIZING CHANNEL WIDTH NEAR STREAM DISTURBANCE ZONE WIDTH2 The near stream disturbance zone width serves as an estimate of the bankfull width This parameter is used to determine the distance of the near stream vegetation to the wetted channel In essence the near stream disturbance zone allows for positioning of the en a near stream land cover relative to the stream channel A statistical validation of GIS sampled channel width polylines digitized from aerial imagery and ground level bankfull width measurements is available in Figure 5 6 a A a Similarly wetted widths IE wereawan o0n T can be estimated using aerial i E imagery Because wetted i widths are highly dependent on Nestucca River downstreanmMeadow Lake instream flow conditions field a verification data must be used TTools has the capability to sample the NSDZ The image below illustrates the digitized right and left channel edges for a section of stream red lines The blue dots in the image below indicate the 100 foot stream reaches 3 ae ee ie Ea T wht Ae gt ae ee 3 2 0 y gt T y gt Pe path bei 2 d 5 cae MOR bon FIGURE 5 16 Channel Width Polylines Digitized from Aerial Imagery Wilson River Oregon 20 Near stream disturbance zone width is the measurement of
67. 7 Shrubs 2 Grasses 75 5 9 5 5 5 5 5 5 5 5 5 5 5 5 5 J 5 7 7 2 2 7 7 324 Developed Residential buildings 100 324 Developed Industrial buildings 100 325 a 0 0 0 325 Pipeline 0 0 0 0 0 3254 WWTP 0 00 3 00 oi NI NININIOIO O1 01 01 OoOo O1 wI RO co CO O H OO ma OO mA O Page 173 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 The image below demonstrates the codes assigned to riparian feature polygons It is essential that each and every polygon within your riparian vegetation polygon layer has a value associated with it The value MUST also be a number and not a string oe SS CONVERTING THE RIPARIAN POLYGON THEME INTO A GRID Now that you have completed the riparian vegetation mapping you must convert the polygon theme into a GRID so that TTools can sample it Here is the way to do it 1 Make sure that your riparian vegetation polygon theme is in the projection that you want to use TTools in Since re projecting grids requires Arclnfo you may not have the ability to do so Thus whatever projection your mosaic DEM is in will determine the projection that you will be using TTools in Turn on the Spatial Analyst extension if you have not already done so Select your riparian vegetation polygon theme
68. 9 The ambient reflection component is modeled using an estimation of average longwave energy emitted from bank side vegetation and the reflectivity of natural water at normal viewing angles i e 4 Variable near stream land cover and topography over the survey extent can alter the reflective component However the reflected energy from the stream surface is 4 or less of the energy received at the sensor If reflections from land cover were not accounted for the calculated apparent temperature of the water could potentially increase by 0 4 C Kay et al 2001 Including a calculated estimate for the reflected component received at the sensor improves the absolute accuracy of the radiant temperature For validation purposes the calibrated radiant water temperatures are then compared to in situ measurements from the instream data loggers at the time of the over flight If a consistent difference is observed between the radiant temperature and the in stream temperatures the atmospheric transmittance as the most sensitive variable is adjusted to provide a more accurate measurement of temperature The resultant accuracy is then reported for each airborne TIR survey as a validation statistic that quantifies error In most cases the radiant temperatures are further validated against independent instream data collected by various federal and state agencies as part of ongoing monitoring efforts Stream temperatures are sampled from the imagery through
69. A dw Wg Z dwy 3 4 Wetted Perimeter Pw We 2 dw v 1 Z 3 5 Bottom Width We Wer 2 Z dep 3 6 Average Bankfull Depth W d Z BF T DT 3 7 Bankfull Depth der dsp _ _ _ _ 3 8 _ ee We Wetted Width Average Wetted Depth a Ww W Ww dw He Me oy d 3 10 Flow as a Function of Wetted Depth and Other Known Values for Trapezoidal Channel form of Manning s Equation 2 _dw Ws Z dw E 3 11 We 2 dw v1 2Z Page 74 Chapter IIl Dynamic Mass Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Wetted Depth Calculation Performed with a Newton Raphson Method The Newton Raphson method offers a computationally efficient procedure for determining the root of a complex mathematical expression Solution for wetted depth represented in Manning s equation 3 11 offers an application for the Newton Raphson method that excels over other iterative methods Below is the technique employed throughout the model to calculate the wetted depth from other wetted dimensions and instream hydraulics This slope predictor method projects the value of the root by estimating from the first derivative of the function and can quickly converge on a solution stepwise Step 1 Write the function so that all variables are on one side and compute first guess of F dw Recall 3 2 2 1 Q A Uas Ay
70. CTION Heat Source allows the user to select the alluvium temperature for stream bed conduction Recall that stream bed conduction is dependent on the stream bed temperature substrate conduction layer temperature as well as the water column and underlying alluvium temperatures For a comprehensive review of these methods see Section 2 3 Substrate Conduction Flux Important e The alluvium temperature will serve Beene Stream Bed Conduction as the conduction Continuous Data Stream bed heat transfer to the water column is complex temperature below Heat is gained by the stream bed from solar radiation that the substrate Mass Transfer Data passes through the water column Further heat exchange via conduction layer T conduction occurs between the stream bed gt water column and stream bed underlying alluvium Alluvium temperatures Associate Wid are needed to calculate the later BankFull Morph _Barkfull Morph Alluvium Temperature 12 PC Evaporation Bed Conduction This value will be used for conduction between the steambed layer and surrounding alluvium below the stream bed Flow Routing a Y Info General Model Input Model Setup Executables Diagrams Clear Sheets Asoraonate model use an at and application are the sole responsiouity of fhe oe a J Department of ine i k GOuUrce Environmental eal BT DEQ Hide Main Menu cage Page 119 Chapter IV Model Operation Analyti
71. DRAULIC FLOW ROUTING Dynamic water routing methods are based on simultaneous solution of the St Venant equations for continuity and one dimensional momentum Numeric methods are available that approximate solutions two these governing equations Two such methods are developed and utilized in the Heat Source model and the approximation methodology is discussed in detail in this section The user has the choice of using either the Muskingum Cunge method or explicit finite difference method for dynamic hydraulic flow routing approximation The Muskingum method uses storage assumptions to calculate the storage terms in the continuity equation Cunge 1969 modified this method to take the finite difference form of the kinematic wave equation and thus incorporate the conservation of momentum The Muskingum Cunge method is a computationally efficient numerically stable physically based numeric approximation It is less sensitive to bathometric data gaps or inaccuracies when compared to the explicit finite difference approximation forms of the St Venant and momentum equations The three point centered difference form of the explicit finite difference numeric approximation of the continuity and momentum conservation equations offers a straightforward finite element derivation Due to stability limits the numerical approximation scheme is less computationally efficient than the Muskingum Cunge method The time step used for the model is dynamic to minimiz
72. Distance Step m dt Model Time Step s n Manning s Roughness Coefficient S Stream gradient unitless t Time s x Longitudinal Distance m Calculate A Cross Sectional Wetted Area m Ck Wave Celerity 2 C C3 Muskingum Coefficients D Diffusion Coefficient Mm dw Average Water Column Depth m K Travel time Parameter s Ry Hydraulic Radius m 3 Q Flow Rate 2 S Storage m U Average Flow Velocity X Wedge Weighting Coefficient Ww Wetted Width m 3 3 2 EXPLICIT FINITE DIFFERENCE METHOD The derivation of the explicit method for flow routing based on the equations of continuity and conservation of momentum originated with Stoker 1957 and Issacson et al 1956 While derivations of the finite forms are limitless and computational power has increased dramatically the basic approach for approximating solutions using the explicit method has remained unchanged The following example is for a three point central difference approximation The governing equations are the St Venant equations Recall the Continuity Equation form 2 3 13 w pa EU X ot Odw Ox 0 Recall the Conservation of Momentum Equation 3 14 oU ot Ox j U Ody g g So S 0 OX The procedure for approximating the continuity equation and the conservation of momentum equation follows basic finite approximation schemes The partial derivatives are written in three point finit
73. EFFECTIVE SHADE DEFINED AND DESCRIBED Stream surface shade is an important parameter that controls the stream heating derived from solar radiation Recall that solar radiation has the potential to be the largest heat transfer mechanism in a stream system Human activities can degrade near stream land cover and or channel morphology and in turn decrease effective shade It follows that human caused reductions in stream surface shade have the potential to cause significant increases in heat delivery to a stream system Stream shade levels can also serve as an indicator of near stream land cover and channel morphology condition For these reasons stream shade is traditionally a focus of stream temperature analysis Table 1 1 Factors that Influence Stream Surface Shade Blue Not Influenced by Land Management Red Influenced by Land Management Season Time Date Time Stream Morphology Aspect Channel Width Incision Geographic Position Latitude Longitude Topography Land Cover Near Stream Land cover Height Width Density Solar Position Solar Altitude Solar Azimuth In the Northern Hemisphere the earth tilts on its axis toward the sun during summertime months allowing longer day length and higher solar altitude both of which are functions of solar declination i e a measure of the earth s tilt toward the sun Geographic position i e latitude and longitude fixes the stream to a position on the globe while aspect provides the st
74. HANNEL EDGES Follow these steps if you could digitize the NSDZ even if there are some stream reaches that you could not You need to create the buffer to extend 300 feet from the bank edges not from the stream center line 1 Add you Right Bank polyline and your Left Bank Polyline to your view 2 Inthe View menu select the Properties option and make sure that your map units correspond to those of the projection you are in 3 Make sure that you have the Xtools not Tools extension installed and turned on You can download this free extension from the Oregon Department of Forestry website at http www odf state or us In the Xtools menu select the Merge Themes option When asked which theme to preserve output from choose either your Right Bank polyline theme or your Left Bank polyline theme 6 When asked which theme to merge with choose the other bank polyline theme 7 Name the output file this is a temporary file that you can eventually delete after this 8 Go to the Theme Create Buffers If this option is grayed out you probably have not set your view and map units 9 Choose your merged banks theme that you just created 10 Choose At a specified distance and type in 300 11 Set the Distance Units to feet 12 Select In a new theme and name the new file Now you have a buffer that will be the basis for your riparian vegetation map Since you have digitized the banks
75. Inflows C U Average Flow Velocity Us Shear Velocity 2 V Water Column Volume m VD Land Cover Density unitless Vsea Substrate Volume in Conduction Layer m Vu 0 Water Volume in Conduction Layer m VoL Conduction Layer Volume m Vw Water Reach Volume m We Bottom Width m Ww Stream Surface Width m W D Bankfull width to depth ratio dimensionless f W Wind Function 2 W Wind Velocity Measured at 2 meters Above Surface 2 Ws Wind Velocity Measured at Water Surface X Wedge Weighting Coefficient Vic Land Cover Shade Density unitless Y Year If month is less than 2 then Y Year 1 Z Channel Side Slope Ratio dimensionless Z Elevation m Zg Zero Plane Displacement m za 0 7 Hic Zo Roughness Height m za 0 1 Hic Zm Measurement Height 2 m Zy gt Zq Zg Z Stream Elevation m Symbols Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 References Adams T A and K Sullivan 1990 The physics of forest stream heating a simple model Timber Fish Wildlife Report No TFW WQ3 90 007 Washington Department of Natural Resources Olympia Washington Anderson D A J C Tannehill and R H Pletcher 1984 Computational Fluid Mechanics and Heat Transfer McGraw Hill New York Anderson E R 1954 Energy budget studies In Water Loss Investigations Lake Hefner Studies Technical Report Prof Pap 269
76. Land Cover Positioner 137 Page ii Table of Contents Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 CHAPTER V SPATIAL DATA DERIVATIONS 5 1 Introduction 139 5 2 Geospatial Data Overview 140 5 3 Aerial Imagery Digital Orthophoto Quadrangles and Rectified Aerial Photos 141 5 3 1 Digitized Stream Position from Aerial Imagery 141 5 3 2 Stream Aspect 142 5 3 3 Channel Width from Aerial Imagery 143 5 3 4 Near Stream Land Cover Mapping from Aerial Imagery 145 5 4 Digital Elevation Model DEM 149 5 4 1 Stream Elevation 149 5 4 2 Stream Gradient 150 5 4 3 Topographic Shade Angle 150 5 5 Thermal Infrared Radiometry TIR Temperature Data 152 5 5 1 Overview of TIR Data 152 5 5 2 TIR Data Collection and Validation Methods 152 5 5 2 Interpretation of FLIR Images 154 5 5 3 TTools Sampling of TIR Data 156 5 6 Other TTools applications 156 5 6 1 Stream Sinuosity 156 5 6 2 Meander Width Ratio 157 5 6 3 Entrenchment Ratio 157 5 7 Digitizing a Stream Layer 158 5 7 1 Cleaning and Unionizing a Stream Layer 159 5 7 2 Cleaning the Overshoots 161 5 7 3 Cleaning the Undershoots 163 5 7 4 Unionizing the Cleaned Stream Polyline 164 5 8 Digitizing Channel Width Near Stream Disturbance Zone Width 165 5 9 Digitizing Near Stream Land Cover 167 5 10 TTools Operation 175 Turning on the T Tools Extension 175 Step 1 Segmenting the Stream and Calculating the Aspect 176 Step 2 Measuring Channel
77. MA 1R 4 4 a a 6 ee Fiom Cacher Tren Lk 2 TES aA Aa Ahi ar HETE Dimma i5 ees 13 E a p 0 ce E Logline Hrer 4a 1i GFF ae A Ah Ore 4 Came ogi odie Pif A 51 0 La 0 ce Tbh on A amp LB 4 25 40 24 Alagi I u OF Ard OO ATI Ogee Eii rr La 5 oo s A UTR pE Qe ccclee cece Wil Blt oeoo o Se ccccee We eccee TA mec o ed bee baw Io o DTI ccc ATT o DAIT of SSSI o Lud aa 4 Sa Q Jamy on AE 5 ibe mld drai UAW rt Eia 2 DT des UEN 73 f T oe 0 i 0 Trib on LB T fre a7 G4 wiam ay A or 12 Diamo AST ee aa 7 GRE 1a o O Hig al oer B en ar 0 arpa SF of zE HIIS LETE UEM a i Sida 0 a oO Dower Lisak 4 J mA ArT MODA Ari c E pje Oe 4 HA Jh j Lu ia a a Tris and Seng 10 aa 35 8 Ad ee Sl oir LE Otis ET EM an 10 HIEL g g u Wierd Lake Tn W arb Jard eve TOLL A Urt CEJA DHAS SA UES Pii WW HY a 0 Tt on U8 iz 4G at 2a Crear an Au Dr 5P DW oe UEMA 79 12 i a a Lake Comek 13 415 7 74 BA 488 Se a oF 6 148 piima Bede OEM EI Ta ia g a QO Tn on LE Ti 442 FELE GAUARI 00 FH Of b t r UMA En UEH a 1d a ful 0 0 0 Sng on FB 15 ate ee tet a ey 20 P of PAETA OE eS E 14 TS 6 o o Tinen Crai 16 SF Feti Aiar Pu ov 7111 O tases FT Oei Jg 10 ETR Q i 5 odes Gresk WV ard of a Ate A p org fil DAUA fy a 34 i FALE 0 0 0 Lasting Pied Feta is Cot nes SFE TIEU Pd Ofz LoS OMe Bee Oe 3 wW GEA a Spang an LA 19 mg pe Kee Fon oF fae OUJDA Redes DEMA E S54 Q 0 Oo prg an Li a Ak Wiig Ari 7 a Drd Saeed Oe Sosa Oe cab UL g 0 P Beta om PA d
78. Mass Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 cL cL cL a ah i FURA Sampe Thes a i oi August g 1999 S 6 e EA o e a n N Klamath z 2 s 21 1 z lhe Thermal Infrared Data 5 15 6 instream Monitoring Data 5 10 0 Flow Direction ete Be Se dm Au A CEN fh CBRL aa a GS Se at TS ho 0 River Miles Therma nirared Over Milti cli gt p a Ther mal if rare Color Map 209 APC LF 1PC 1 ls ea 10 C d z FIGURE 3 9 Above Instream and TIR Monitoring Data Below An Example of TIR Imagery Cooling from a Spring River Miles 80 41 to 80 65 Williamson River Oregon Page 89 Chapter Ill Dynamic Mass Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Thermal Infrared Over Muki Spectral Image Thermal Infrared Color Map in i hy SS ae Pak i 3 T 15 Diversion FIGURE 3 10 Water Withdrawal and Return Flows Located and Measured with TIR remote sensing Williamson River Oregon Water volume losses are often visible in TIR imagery since diversions and water withdrawals usually contrast with the surrounding thermal signature of landscape features see Figure 3 10 Highly managed stream flow regimes can become complicated where multiple diversions and return flows mix or where flow diversions and returns are
79. Methodology Robustness Heat Source was born out of the exploration of the causal factors that affect dynamic thermal regimes with a focus on the data and methods suited for riverine thermodynamics and hydrodynamics that capture complex analytical procedures robust and comprehensive methods and considerations for the interrelatedness between parameters Important processes are included in the methodology such as mass transfers from tributaries groundwater inflows landscape thermal radiation adiabatic cooling robust radiation modeling multiple evaporation methods and complex hydrodynamic routing with hyporheic exchange within the substrate to name a few Very few efforts of simplification are evident in the methodology and instead the inclusion of all complex processes is generally the guiding principle in the methodology development and application Aside from computational speed analytical modeling can be performed using deterministic methods over relatively small time and distance finite difference steps Model operation resolution should match the dynamic nature of stream temperature that tends to occur over small scales across a variable landscape and sometimes in a brief period of time High Resolution Application of the Methodology By design spatial input data is derived and sampled at a high resolution offering a second source of robustness This method of stream temperature simulation minimizes assumptions and includes all i
80. N Latent Heat L Evaporation represents the difference in enthalpy of the air near the water surface and the ambient air Evaporation raises the total energy content of the air near the evaporating surface representing a heat loss to the water column As the molecular motion of a water molecule in the liquid phase increases in response to increased heat energy and aerodynamic energy it begins to overcome the molecular attraction to liquid water causing water molecules to escape as water vapor When the vapor pressure of the air above the stream is low the released water vapor from the stream has a lower chance of colliding with other molecules in the air a greater chance of volatilizing away from the water column surface and thus a greater chance of remaining in the gaseous phase as water vapor If the vapor pressure is high the chance of molecular collisions is greater with a decreased tendency for the water vapor to remain volatilized into the liquid phase Saturation vapor pressure occurs when the air mass contains the maximum water vapor content determined as a function of air temperature Attainment of a saturated air vapor pressure implies that the rate of water molecules leaving the stream surface is equal to the rate of water vapor molecules being introduced back to the liquid phase of the stream Under this condition evaporation stops Condensation is the reversal of evaporation and instead the delivery of water vapor molecu
81. RADIAL LC VALUES This worksheet macro will calculate whether radial sampled land cover and water sampled values will fall within or outside the channel boundary following a change in bankfull width Points that are not within the bankfull channel are denoted with LC for Land Cover and points that fall within the bankfull channel are denoted with W for Wet A comparison of the current and the new channel width output made by the macro for you identifies the Dried no longer within the bankfull channel and the Wetted now in the bankfull channel locations You can then search for these values Dried and Wetted and make appropriate changes for example associate the nearest neighboring value Input Condition Output Condition Sample Points that NE were previously Bankfull Width within the bankfull Reduction dimension Page 138 Chapter IV Model Operation Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Chapter Spatial Data Derivations TTools Input Data Procedures and Methods Aeri al Photos Spatial Data Derivations Involved Automated Sampling of Spatial Databases and Performing Simple Calculations 5 1 INTRODUCTION TTools 7 0 is an ArcView extension developed by the Oregon Department of Environmental Quality This ArcView extension contains a suite of tools designed to automatically sample spatial data sets
82. Reflectivity unitless Reflectivity of Stream Bed if Direct Beam Radiation unitless Reflectivity of Stream Bed if Diffuse Radiation unitless Radius Vector radians Volumetric Weighted Density Storage m Friction slope unitless Shadow Length Cast from each Zone m Approximation of the Slope S Air Mass Transmissivity Direct Beam Transmissivity of Water Column unitless Diffuse Transmissivity of Water Column unitless kg m s Julian days since epoch 1900 January 0 5 ET Julian centuries since epoch 1900 January 0 5 ET Daylight Savings Time day fraction Greenwich Mean Time day fraction Solar Time minutes Time Zone see Table 2 1 Air Temperature C Shear Stress Subsurface Inflow Temperature y C Surface Inflow Temperature C Water Temperature C Symbols Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 SYMBOLS AT Change in Conduction Layer Temperature from Solar Radiation C ATE Change in Conduction Layer Temperature from Conduction C To Conduction Layer Temperature C Tae Conduction Layer Temperature Accounting for Solar Irradiance C TE Conduction Layer Temperature Accounting for Conduction C Tew Subsurface Inflow Temperature C Tin Surface Inflow Temperature C Tour Withdrawal Flow Temperature Ty C Trig Instantaneous Flow Weighted Temperature of Surface
83. River Mile FIGURE 3 11 Mass balance developed using instream gage data TIR temperature data and water rights data North Fork Sprague River Oregon 16 In this case potential flow rate refers to the flow condition that would exist without anthropogenic modifications withdrawals returns discharges augmentation Page 91 Chapter Ill Dynamic Mass Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 DISCUSSION OF ASSUMPTIONS AND LIMITATIONS FOR TIR DATA BASED MASS BALANCE METHODOLOGY Small mass transfer processes cannot be accounted since TIR data often has an accuracy of 0 5 C A limitation of the methodology is that only mass transfer processes with measured ground level flow rates or those that cause a TIR quantifiable change in stream temperature with the receiving waters i e identified by TIR data can be analyzed and included in the mass balance For example a tributary with an unknown flow rate that cause small temperature changes i e less than 0 5 F to the receiving stream cannot be accurately included This assumption can lead to an under estimate of influent mass transfer processes Limited ground level flow data limit the accuracy of derived mass balances Errors in the calculations of mass transfer can become cumulative and propagate in the methodology since validation can only be performed at sites with known flow rates These mass balance pr
84. There could be a variety of reasons For this Check your input data or try decreasing time step and or increasing distance step Press OK to ignore and Cancel to stop the model Cancel FLOWS ARE APPROACHING ZERO MODEL OPTIONS A method is developed in Heat Source that allows flow volumes to reach zero without model failure i e division by zero errors Heat Source will notify the user once stream flows have reached cfs 0 0071 cms or less and will ask whether the operator would like to continue This message is basically asking the user whether the low flows being simulated reflect the true condition At this time the model operator can either stop the model run or continue the simulation The model will not ask the user again about encountered flow volumes for the duration of the simulation Once a user selects to continue the simulation the model simply skips the stream nodes without sufficient flows to route i e less than cfs In these stream nodes hydrologic and heat processes are not calculated and output variables are assumed to be zero Proceeding downstream the model will detect when flows become sufficient to commence flow routing again i e greater than 1 4 cfs Of particular concern is the estimation of the water temperature in this first stream node below the dewatered section where flows are sufficient for flow routing and heat transfer modeling In essence this stream node represents a bound
85. Unresolved questions will remain when you are finished with your analytical effort While our ability to measure and quantify landscape and hydrologic processes has dramatically improved over the last decade there remain several limitations for some parameters and these are often compounded by the limited resources often available for these analytical efforts Therefore we simply cannot address stream temperature in all of its complexity Although analytical modeling is helpful in understanding the interrelated hydrodynamic and thermodynamic processes associated with stream temperature it is not a panacea Let me quickly explain before you toss this document in the recycling bin While many heat and mass transfer processes are well understood and even easily measured and independently modeled at various levels of complexity i e flow shade humidity wind speed etc the variation and interdependence of some of these parameters across a drainage is poorly documented For example near stream microclimates that control humidity wind speed and air temperature are a function of the near stream land cover type and condition as well as topography and atmospheric processes Since the physical attributes of both land cover and topography vary in spatial distributions often dramatically we should assume that microclimates also vary across the landscape Spatial variability is compounded by the temporal variation associated with atmospheric parameter
86. a nodes enemas Double Click e A more typical Select number of continuous data sites number of nodes ee would be roughly one Bankfull Morph el per ten kilometers ji ae e Data availability Evaporation gt You must setup the continuous largely determines the Bed Conduction WR data sheet before you can run any number of alow seuline Cee eS Continuous Data Nodes Required for All Models ae Clear Sheets Asoraonate model use and anoication are the em a a sole responsiblity of fhe Se ys t user Department of e do a ree Environmental Quality an ue jj rii a a 3 ha k F Eoo 7 a b B og Hide Main Menu CONTINUOUS DATA NODE LOCATIONS Continuous data node locations must be associated with longitudinal positional data i e stream KM in the upper headwaters to lower mouth downstream direction Continuous Node number 1 is the data site that will be used for atmospheric data until the model simulating in the downstream direction encounters the next continuous data node where the data associated with that node will then be used as atmospheric data Climatic variations such as Page 105 Chapter IV Model Operation Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 microclimate adiabatic air temperature effects etc should be represented in the continuous data BOUNDARY CONDITIONS The stream temperature boundary con
87. a predictor corrector approach to approximation of the non uniform one dimensional advection dispersion partial differential form Figure 2 6 displays the MacCormick solution scheme In summary the approximation uses two forward slope predictions along with Euler s method and then averages the slope predictions to calculate a backward difference Chapra 1997 The MacCormick method is computationally efficient more stable than traditional explicit approximation solution methods and does not introduce numerical dispersion since the method uses a time centered approach Chapra 1997 note that the MacCormick method is particularly accurate since it employs a time centered and space centered approach A potential limitation is conditionally stability However stability greatly exceeds that offered in explicit methods and approaches constraints more commonly found with Euler s method Numerical stability criterion cannot be calculated suffice to say it will be apparent when stability limits are exceeded the model will fluctuate temperature prediction wildly and then crash Forward First Approximation t of the Slope MacCormick 1969 t t s U Wit wi dx sD Twin 2 Twi Twi dx total J 2 119 Pho Cho dw Forward First Approximation t Using Euler s Method for Predictor Calculation MacCormick 1969 Tu Ty 84 at 2 120 Page 68 Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mas
88. abitgis html Page 116 Chapter IV Model Operation Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Morphology Data Worksheet Substrate Information Horizontal Bed Conductivity from Bedient amp Huber 199 Sit 0 02 mms 0 00079 ints Gravel 6 0 30 mms 0 236 1 16 im Sand 0 02 6 0 mme 0 00079 0 236 ints Cobble 30 mms 1 18 init Bed Particle Size from Bedient amp Huber 1992 Rosgen 1996 Sit 0 062 mm C 0 0024 in Gravel 20 63 5mm 0 0767 2 5 in sand 0 062 2 0 mm 0 0024 0 078 in Cobble 63 5 254 mm 2 5 10 ind Percent Embeddedness Simonson et al 1994 106 Rocks are completely surrounded by sediment and completely covered by fines T5 Rocks are completely surrounded by sediment and half covered by fines 509 Rocks are completely surrounded by sediment but are not covered by fines 25 Rocks are half surrounded by sediment and are not covered by tines i Important Horizontal Bed e You must input substrate information Either use Conductivity Bed Particle Embedded stream survey information or assume values mm s Size mm ee based on your knowledge of the substrate types THERMAL INFRARED TIR DATA Thermal infrared stream temperature data serves as a valuable tool for model validation Input of these data is optional however it is strongly recommended by the authors that e
89. ace As Ng Pw 3 35 Seepage Face Thickness hs dx S 3 36 Hydraulic Head Calculations hp dw 3 37 hpi dwi dX So dw dx So S 3 38 Composite Substrate Hydraulic Conductivity Ks Kg 1 Ce K_e Ce 3 39 Page 96 Chapter IIl Dynamic Mass Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Variables Measured Known Cg Embeddedness dx Model Distance Step m Ks Dominant Substrate Hydraulic Conductivity Ke Embedded Substrate Hydraulic Conductivity for Silt Sand S Stream gradient unitless Calculate A Cross Sectional Across Seepage Face m Ks Composite Substrate Hydraulic Conductivity hp Hydraulic Head for Darcy Calculation m hs Hydraulic Head Across Seepage Face m dw Water Column Depth m Pw Wetted Perimeter m Qhyp Hyporheic Exchange Rate Across Seepage Face a S Friction Slope unitless 3 4 0 EVAPORATION LOSSES Loss from the mass transfer liquid phase change to gas associated with evaporation calculated in order to account for heat transfer from the water column is included as a negative term The rate of water loss that accompanies the phase change and mass transfer from water column to the overlying air mass is a function of the evaporation rate and water surface area The evaporative process is described in detail in Section 2 4 1 Goan E Ww dx 3 40 Variable
90. ace 1 _ Ws Wind Velocity Measured at Water Surface Zero Plane Displacement m ea Za 0 7 Hic a Roughness Height m O za 0 1 Hic Measurement Height 2 m L es Zq Zo 2 5 CONVECTION FLUX convection The convection heat flux also known as sensible heat at the air water interface is the result of turbulent and molecular heat exchange that occurs in response to a heat energy gradient Sensible heat will be transferred between water and air when the respective temperatures are different From Furrier s heat transfer studies the rate of heat energy transfer is proportional to the heat gradient McCutcheon 1989 The Bowen ratio is a constant of proportionality between the convection flux and the evaporation flux at the air water interface and is therefore a function of stream and air temperature and vapor pressure Bowen 1926 It follows that the convection heat flux at the air water interface is the product of the Bowen ratio and the evaporative heat flux Convection Heat Flux Bowen 1926 P convection Br evaporation 2 111 Variables Calculated Br Bowens Ratio Defined in Equation 2 102 unitless convection Convection Flux gt P evaporation Evaporation Flux Defined in Equation 2 94 Page 64 Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 2 6 STREAM TEMPERATURE SIMULATION METHOD 2 6 1
91. al Analyst to sample a grid theme Spatial Analyst can perform a limited number of commands in a given ArcView session before causing a Segmentation Violation and crashing ArcView Therefor it is strongly recommended that you save the project completely close out of ArcView and re open the project before beginning this step of TTools Doing so will clear ArcView and Spatial Analyst memory and TTools will then be able to accurately predict and prevent a potentially disastrous crash Page 178 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 PREREQUISITES e You must have your TTools point theme in the view e You must have a mosaiced 10 meter or 30 meter DEM in the view The DEM must cover the entire 4 field subbasin that you are sampling within e You must have performed the Measure Elevation Gradient step of TTools Helpful Hint Before proceeding with TTools sampling make sure that your DEM and TTools point coverage are located on your local hard drive If your DEM resides on a network drive T Tools sampling will take about three times longer STEPS Select the Measure Topographic Shade option in the TTools menu Select your TTools point theme Select your DEM grid theme oe IS When asked to select your DEM elevation units choose the units of the values that are in the actual DEM that you are
92. alytical Methods for Dynamic Open Channel Heat and Mass Transfer SYMBOLS p p p P iongwave Page 184 Oo O oo O convection conduction evaporation Daa Day Ow Ore Oey g P srg P spp D sprg1 P sro P spp Dspp2 D spe D spp3 P spp D sppa spes P spos D spege Dsppe D spe sprpz e G Methodology for the Heat Source Model Version 7 0 Vapor Pressure mbar Saturation Vapor Pressure mbar Vapor Pressure Based on e mb Saturation Vapor Pressure Based on Ty mb Density Gradient 10 Convection Flux ea Substrate Conduction Flux Evaporation Flux 2 Longwave Radiation Flux ae Change in Stored Heat 4 m Water Advected Heat ls Atmospheric Emitted Longwave Radiation Flux 3 Land Cover Emitted Longwave Radiation Flux 2 Water Column Emitted Longwave Radiation Flux Acceleration of gravity 9 8 m s Global Solar Flux 7 Direct Beam Solar Radiation Estimate above Topography Direct Beam Solar Radiation above Topography Ea Diffuse Solar Radiation above Topography Direct Beam Solar Radiation below Topography a Diffuse Solar Radiation below Topography a Direct Beam Solar Radiation below Land Cover a Diffuse Solar Radiation below Land Cover gt Direct Beam Solar Radiation above Stream Surface i Diffuse Solar Radiation above Stream Surface a Direct Beam S
93. an 2 65u Wunderlich 1972 By measuring surface temperature the accuracy of the radiant temperature is not influenced by a transmissive component from the stream bed and is therefore not a function of stream depth TIR images measure the global water temperatures in stream systems where turbulent mixing occurs Torgersen et al 2001 ODEQ 2000 Boyd and Kasper 2002 The instream data loggers that are used to calibrate and validate the TIR images also can be used to confirm that the water column is mixed and that the measured radiant temperatures are representative of the global water temperatures Furthermore visible band color video is collected simultaneously with the TIR images and directly shows areas of obvious mixing such as riffles and rapids Flowing water is inherently mixed from dispersion i e turbulent diffusion and the vertical mixing that occurs from a variable flow profile i e slower velocities occur near the stream boundaries and faster velocities occur away from channel boundaries Martin and McCutcheon 1999 Thermal stratification often develops in areas where little or no mixing occurs such as behind impoundments or in deeper low velocity channels When a stream is stratified TIR measurements represent only the surface temperatures It follows that recognition of a thermally stratified as opposed to a mixed water column will control how TIR images are interpreted Under mixed flow conditions visible shadows have no influen
94. and Boulder gt 254 mm Page 53 Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 may misrepresent local variations Substrate size is typically sieved measured in terms of diameter and quantified as a percentage of the total sampled volume A dso measurement indicates an average alluvium particle size within a sample Embeddedness is a measure of the degree to which substrate is surrounded by fine sediments silt and sand It is assumed that embedded fine sediments occupy interstitial soaces in the alluvium For example 25 embeddedness indicates that approximately one quarter of the void space in the alluvium is occupied by fine sediments Porosity adopted from Bedient and Huber 1992 n 0 3683 dg 1 E lagg B 2 78 where qsand 5 Particle Size of Fines 0 0622 mm d o Sediment Particle Zone mm E Embeddedness unitless 50 n 0 3683 dso 1 E lasg Bf 45 R2 0 965 FIGURE 2 5 40 Estimated Porosity n 0 Embeddedness Values as a Function of O ni Alluvium Particle Size and S 35 ee EINE OSCRNESS Embeddedness Values 50 Embeddedness from Bedient and Huber 75 Embeddedness 1992 30 Neel tele 2006 SS 0 50 100 150 200 250 Particle Size dsp mm Since both water and alluvium occupy the conduction interface the thermal conductivity Ko is calcu
95. and Cover Species and Physical Attribute Data Collected in 1999 Measured Land Cover Height ft os g q104 8 PIOUIWIeIS qniys puea Mm qniys pueyuq S1a 1uoyD snonpiseq Jediunr Ula Sa FIGURE 5 8 Example of Near Stream Land Cover Ground Level Monitoring Sites and Summarized Physical Attribute Data Williamson and Sprague Rivers Oregon These data allow the near stream land cover classifications to be associated with local physical attribute information specific to the basin of interest oe 80 Was 70 TEA mi 60 pju l i oOo ee 50 5 baa i HE ES 2 40 i w 30 E T p Eg 2 6 2 104 o FIGURE 5 9 Near Stream Land Cover Height Upper Williamson River Oregon Page 148 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 5 4 DIGITAL ELEVATION MODEL DEM Spatial data sets derived from DEMs include e Stream Elevation e Stream Gradient e Maximum Topographic Shade Angles East South West The Digital Elevation Model DEM data files are grids in which each cell contains a land surface elevation value The U S Geological Survey as part of the National Mapping Program produces these digital cartographic geographic data files DEMs typically have either a 30 meter cell size or a 10 meter cell size DEMs are used to determine stream elevation stream gradient valley gradient vall
96. annel that will accommodate flows Heat Source Channel Morphology xj The wetted width is exceeding the BFW at river KM 31 64 to 31 74 To accomodate flows the BF area should be 1 67 or greater Select es to continue the model run and use calc wetted widths or select No to stop this model run suggested Area values will be recorded in Column z in the Morphology Data worksheet Do you want to continue this model run 4 8 OTHER UTILITY APPLICATIONS A utility application with VBA macros is available on the distribution CD as a stand alone program to help manipulate input data To date the Land Cover Poistioner is the only utility application packaged with Heat Source v 7 0 4 8 1 LAND COVER POSITIONER TRANSVERSE TO RADIAL LC VALUES This worksheet macro will radially distribute transverse land cover inputs for Heat Source v 7 0 Ttools v 7 0 samples in a radial pattern and creates land cover data that is formatted for Heat Source In the event that TTools 7 0 is not used to sample land cover or a previous version of T Tools is used to sample land cover values this worksheet macro can transform transverse land cover data into radial sampled data Page 137 Chapter IV Model Operation Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Output Conditing Model Transverse Land Cover Samples Land Cover Samples UPDATE
97. ansfer of heat energy is the summation of the rate change in temperature due to heat energy thermodynamics advection and dispersion Given that the stream is subject to steady flow conditions and is well mixed transverse temperature gradients are negligible Sinokrot and Stefan 1993 An assumption of non uniform flow implies that cross sectional area and flow velocity vary with respect to longitudinal position Unsteady flow assumptions allow for flows velocities and wetted dimensions to change over time The following second ordered parabolic partial differential equation describes the rate change in temperature for non uniform flow Non Uniform One dimensional Heat Energy Transfer oT T 0 T D FI U ee D M 2 118 K 0X CH 0 Ph o Aw Advection Dispersion Heat Transfer aa Mass Transfer When combined with the dynamic flow routing see Chapter 3 Unsteady Flow 0 Non Uniform Flow 0 X Page 66 Chapter Il Heat Transfer Page 67 Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Variables Measured Known Cho Specific Heat of Water dx Model Distance Step m g Acceleration of gravity 9 8 lt 2 Pho Density of Water 998 2 2j m S Channel Slope unitless x Longitudinal Distance m t Time s Calculated Aw Surface Area m dw Average Water Column Depth m D_ Dispersion Coefficient 15 iota T
98. ary condition The model estimates this stream node temperature as the last known stream temperature value in the closest proximity to the stream node It is likely that this assumption will be minimized since instream flows will be very small relative to the inflows and the inflow temperatures should dominate Heat Source Channel Is Going Dry i x x The channel is going dry at 54 21 river EM The model will either skip these dry stream segments or you can stop this model run and change input data Do you want to continue this model run Page 136 Chapter IV Model Operation Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 CALCULATED WETTED WIDTHS ARE EXCEEDING BANKFULL WIDTHS Both Heat Source and Flow Router calculate wetted channel dimensions If the flows exceed bankfull per the bankfull channel design and flow inputs the model will provide a message that warns the user of potential problems Specifically the user is notified where the location of the first bankfull flow The user can choose to ignore this problem and the model will simply calculate the appropriate wetted width for the flows which will exceed the bankfull width or the user can stop the model run and modify inputs The model will list recommended bankfull cross sectional areas in column Z in the morphology data worksheet By changing W D or channel side slope Z the user can create a ch
99. at occur over longer distances than discrete subsurface inflows i e a spring The temperature of the accretion flows along with the flow rates should be input in columns E gt F in the Flow Data worksheet When accretion flows are close enough so that more than one occurs in a model distance step the accretion flow rates will be summed and a flow based average accretion temperature will be derived and used in the mixing calculations Important Zero values indicate that no accretion flow is occurring FLOW WITHDRAWALS Withdrawals can be entered to represent known flow losses such as diversions from the stream or other human caused flow reductions Withdrawal flow rates are assumed to remain constant throughout the simulation period Withdrawal flows should be input in column G in the Flow Data worksheet When withdrawal flows are close enough so that more than one occurs in a model distance step the withdrawal flow rates will be summed Important Zero values indicate that no withdrawal is occurring DELETE INFLOW DATA A message box will ask the user to confirm that they want to delete existing inflow data Configuring the number of inflow data sites data involves changing the entire Inflow worksheet If the user can keep track of existing data associations it may be easier to choose not to delete existing data and simply move it appropriately after the continuous data setup configuration If the setup involves significant
100. ata sets for stream networks simulate dynamic hydraulics and thermodynamics Appropriate use and application are the sole responsibility of the user This document may be downloaded from the web site at the following URL http Awww deq state or us wq TMDLs tools htm Updated February 12 2003 amp February 20 2007 Cite this document as Boyd M and Kasper B 2003 Analytical methods for dynamic open channel heat and mass transfer Methodology for heat source model Version 7 0
101. ate of heating is less in the forested reach than in the meadow reach This discussion of semantics is necessary simply because the terms heating and cooling are used so frequently without reference to the dimension space or time over which the change is occurring Statements are often made that shade cannot cool water but instead shade only reduces stream warming Sucha generalization is true as long as the dimension of change Is time Spatial representations of shade induced stream temperature change can however represent cooling gradients see Figure 1 5 It becomes easy to see that as streams heat over time at variable rates that actual temperatures at specific locations will be different With this background the temperature change over distance will likely represent cooling gradients in shaded stream reaches In this context the generalization that shade does not cool water is in fact incorrect overly simple and poorly defined Aside from the terminology of heating and cooling we do not want to lose focus of the primary finding represented in the temperature and shade comparison The lack of shade correlates to warmer stream temperatures This finding is consistent with the literature and theoretical constructs of stream temperature dynamics Spatial and Temporal Stream Temperature Profile Changes Tiya aL Direction of Flow Forested Meadow Reach Reach O 6 i i p T S e mile mile AX oS 1 3 O AT lt qt
102. ation and mapping process DELINEATING RIPARIAN LAND COVER POLYGONS Vegetation mapping should be done using the highest resolution and most recent aerial imagery available Streams change over time and so does the riparian vegetation Higher resolutions allow you to see more detail such as smaller willow galleries along a stream bank Multispectral or color imagery enhances the vegetation mapping process by making the various riparian communities more decipherable A typical view extent for mapping riparian vegetation is between 1 2 500 and 1 5 000 maximum The image below shows an example of mapped riparian features along the Williamson River in southern Oregon Mapped features in this image include a road house farm field willows along the bank grassy areas dense conifer stands less dense conifer stands and the river itself The basic rule of thumb when delineating riparian vegetation polygons is to identify areas with the following three distinctions 1 Species Composition 2 Canopy Density 3 Height Page 170 Chapter V Spatial Data Derivations n ee ae w S 8 9 Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Gy SRS MW REAR ei E Ole Dio atleast ae It may be difficult to identify species and heights from the aerial imagery but that is where GROUND LEVEL DATA comes into play It is critical that you have collected a sufficient amount
103. be interpreted from the aerial imagery 5 9 DIGITIZING NEAR STREAM LAND COVER You must have digitized your stream polyline and the channel edge NSDZ polylines before attempting to digitize vegetation TTools uses your digitized stream polyline as a reference point for sampling vegetation CREATING THE BUFFER IF YOU COULD NOT DIGITIZE THE CHANNEL EDGES Follow these steps if you could not digitize the NSDZ anywhere along your stream You need to create a buffer that extends 300 feet from the stream center line Add your digitized stream theme and the aerial imagery to your view 2 Inthe View menu select the Properties option and make sure that your map units correspond to those of the projection you are in 3 Inthe Theme menu select the Create Buffers option If this option is grayed out you probably have not set your view and map units Choose your stream polyline theme Choose At a specified distance and type in 300 Set the Distance Units to feet a oo oS Select In a new theme and name the new file Now you have a buffer that extends 300 feet from your digitized stream The next step will be to cut that buffer into multiple polygons that represent the riparian vegetation Page 167 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 CREATING THE BUFFER IF YOU COULD DIGITIZE THE C
104. bs to such a thermal stress depends on the temperature that the fish is acclimated as well as particular development life stages This cause of mortality termed the incipient lethal limit results from breakdown of physiological regulation of vital processes such as respiration and circulation Heath and Hughes 1973 The most common and widespread cause of thermally induced fish mortality is attributed to interactive effects of decreased or lack of metabolic energy for feeding growth or reproductive behavior increased exposure to pathogens viruses bacteria and fungus decreased food supply impaired macroinvertebrate populations and increased competition from warm water tolerant species This mode of thermally induced mortality termed indirect or sub ethal is more delayed and occurs weeks to months after the onset of elevated temperatures in the mid 60 F to low 70 F 17 8 C 22 C The temperature needs of aquatic organisms are used largely as a primary design criterion for water Cold water fish population protection and rehabilitation temperature regulatory is the primary purpose for stream temperature programs Summertime assessments and modeling Conclusions based on temperatures tend to analytical outputs should relate back to salmonid life target sub lethal ranges stage thermal ranges see table below Page 24 Chapter Introduction Page 25 Analytical Methods for Dynamic Open Channel Heat and Mass Trans
105. c flow routing method under the Flow Routing tab 4 3 1 GENERAL INPUTS The first step in the model setup is to enter the general information that will be used to setup input data sheets control the model simulation length and finite difference time and distance steps To access the Main Menu click on the Main Menu buttons located on most worksheets except those containing charts and then select the General Model Input tab Enter the data with attention to units of measurement The Time Inputs list drop boxes contain the input information for the simulation per and the time zone Selections are made by double clicking and should be done after the other inputs are entered The information entered as General Model Inputs will be visible on most of the worksheets except those containing charts listed as Simulation Information Important Info General Model Input Model Setup Executables Diagrams Do not change the General Model Input General Model Inputs on the Name Bear cree sss Bear Creek worksheets Instead Starting Dat meee 3 14 1999 Time Inputs use the text boxes Stream Length km 32 04 Simulation Period and list boxes found Days Time Zone under the General Model Inputs tab in em the Main Menu Central East e Be exact when i i entering stream Flush Initial Condition days 5 Double Click length and longitudinal sampling distance e Make sure
106. cal Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 4 3 10 MODEL SETUP PHYSICALLY BASED FLOW ROUTING METHODS Two flow routing models are available Muskingum Cunge Flow Routing and Explicit Hydraulic Model Routing Each method has strengths and weaknesses as outlined in Table 3 1 Summary of Muskingum Cunge and Explicit Finite Difference Methods If using the Muskingum Cunge Flow Routing method the user will have the chance to have the model calculate the Muskingum Storage Factor X which simplifies the model inputs and is physically based One drawback may be a reduction in calibration parameters Aside from the Muskingum Storage Factor X user s should use morphology and roughness parameters to calibrate flow routing Important Info General Model Input Model Setup Executables Diagrams Carefully select the mass transfer Data Sheets Physically Based Flow Routing Methods methodology based Continuous Data Muskingum Cunge a on the model Highly stable flow routing method that allows for simplified application Mass Transfer Data bathymetry data Can be calibrated with Muskingum Storage i Geleci to Calcuiate Factor W and Manning s roughness coefficient Muski St i ti USKINQUM otorage __Negematc Explicit Method g g associate WDO Multiple stability criteria and variable flow limited method that is Factor x if you are highly sensitive to channel bathym
107. ccount for emergent vegetation in the solar routing calculations eApplication Info General Model Input Model Setup Executables Diagrams Simulate water surface Shade a lat solar exposure and shade a lator Purpose ACE ANATOR effective shade Select Shade a lator to calculate effective shade at the stream Flow Router Fo Inputs All parameters found in the TTools Data Hear anue Shade a lator simulates solar flux values that are are comparable to those measured by a solar pathfinder at the stream surface Simulation occurs over the defined stream network during the worksheet and period specified Output is provided at the defined distance step Cloudiness Column J and can be found on the following sheets Chart Salar Flux i in th ntin Chart Sshade Output Solar Potential and Output Solar D id ware Received ata worksneet Outputs Chart Before you run Shade a lator enter Solar Flux Chart all data found on the Land Cover i Shade Output Solar sheet and run Wegematic Potential and Output Solar Surface Account for Emergent Vegetation Asoraonate model use i and anoication are the oon ae sole responsibility of the Wire Oregon Department of es a aiiai aT ree Environmental n j Hide Main Menu a har ve Page 124 Chapter IV Model Operation Analytical Methods for Dynamic Open Channel Heat and Mass Trans
108. ce when asked if you want to reverse line segments You will need to delete this T Tools point coverage from the ArcView project and start the Segment Calculate Aspect step over The first record in the TTools point theme table Id 0 MUST correspond to your uppermost node nearest the headwaters The remainder of TTools uses this information to determine which direction is downstream STEP 2 MEASURING CHANNEL WIDTHS PREREQUISITES e You must have performed Step 1 of TTools Segment Calculate Aspect e You need a Right Bank polyline theme and a Left Bank polyline theme Both must have been cleaned and unionized like your stream polyline was e The bank polylines must extend the full length on both sides of your TTools point coverage i e extend the entire length of the stream STEPS 1 Select the Measure Channel Widths option on the TTools menu 2 Select your TTools point theme 3 Select your Right Bank polyline theme 4 Select your Left Bank polyline theme 5 When asked whether to overwrite existing data If you choose Yes all channel width data will be erased and re sampled If you choose No sampling will be performed only where there are zero values in the Channel column of the T Tools data table Helpful Hint e The output units in the field titled Channel will be meters e Remember that areas where you could not interpret the NSDZ from the aerial imagery you did not move t
109. ce on thermal infrared signatures at the stream surface Figure 5 13 FIGURE 5 13 An Example of Mixed Stream with Shaded Surface from TIR Image without Differential Surface Heating Faux personal communication Even heavily stratified stream reaches have some level of mixing that is visible where cooler deeper water mixes to the surface around bends instream objects or from wind kinetic energy As a result TIR imagery can be used to Page 154 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 identify thermal stratification Figure 5 14 The presence or absence of a thermal stratification provides information about both flow conditions and stream temperature Over a stream network a portion of the stream segments will tend to display thermal stratification For example of the 442 km stream length surveyed in the upper Grande Ronde River sub basin Oregon a total of 67 km 15 were determined to be thermally stratified ODEQ 2000 Modern TIR sensors have sensitivities from 0 2 to 0 02 C Under thermally Stratified conditions the TIR sensor detects surface temperature patterns that result from slight mixing from wind and flow and differential heating relationships in multiple directions i e longitudinal and transverse Under these conditions differential heating at the stream surface results from large variations in rates
110. ces and the backradiation emission from the water surface OUTPUT EVAPORATION Hourly evaporation heat flux output data at the water surface air column interface OUTPUT CONVECTION Hourly convection heat flux output data at the water surface air column interface OUTPUT CONDUCTION Hourly conduction heat flux output data at the water column substrate interface OUTPUT TOTAL HEAT Hourly total heat flux output data between the water column and the surrounding environment air column and substrate OUTPUT EVAPORATION RATE Hourly evaporation rate output data resulting from diabatic and adiabatic processes Page 132 Chapter IV Model Operation Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 OUTPUT DAILY HEAT FLUX Daily output data are listed in the Output Daily Heat Flux worksheet The daily data that can be found on this worksheet are View to Sky Effective Shade o Potential Solar Radiation Heat Flux o Solar Radiation Heat Flux Above Stream Surface Ga o Solar Radiation Heat Flux Received by Stream gt o Longwave Heat Flux 7 o Convection Heat Flux gt o Conduction Heat Flux 4 o Evaporation Heat Flux o Total Heat Flux Ge 4 6 COMMON SOURCES OF PROBLEMS o Poor Output Resolution Finite difference distance and time steps too coarse o Model Instability Crashes Combinations of f
111. channel width performed by TTools It is named by the authors because there is not an exact reference to GIS sampled channel width that correlates with a commonly used ground level measurement It is intended to serve as an estimate of the bankfull width but the authors acknowledge that measurement limitations may affect the accuracy of this estimate Statistical validation of derived channel widths with ground level measurements is highly recommended Page 165 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 The following steps will guide you digitizing channel width 1 Select your cleaned 1 5 000 stream theme in your view Go to Theme Convert to Shapefile Name the new theme this will be either your right bank or left bank theme Select your new bank theme in your view os W N Zoom to the beginning of your stream at least 1 5 000 You should have your aerial photograph or DOQ turned on as well Go to Theme Start Editing 7 Click on the Vertex Editing tool in your button bar D 8 Now click on your bank polyline with the cursor All the nodes will now be highlighted with a small box see image below 2 ArcView GIS Version 3 1 Eile Edit Yiew Theme Analysis Surface Graphics Tools Window Help Eee Nae AKRA Ae Zhe lel IE E OD eael leei 2 Scale W217 amogic C _ 1030 1237 L 1238
112. ct mixing Page 72 Chapter IIl Dynamic Mass Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Mixing external flows tributaries groundwater inflows point sources etc with a receiving water will change the heat when the respective temperatures are different Mixing simply changes the heat as a function of stream and inflow volumes and temperatures Remote sensing using thermal infrared radiometry TIR can easily identify areas where heat change occurs due to mixing with surface and subsurface waters 3 2 CHANNEL GEOMETRY amp MANNING S RELATIONSHIPS A trapezoidal channel shape can be used to estimate bankfull channel dimensions represented by measured bankfull width Wer and channel side slope ratio Z channel longitudinal slope So and an assumed measured width to depth ratio W D From these known values it is possible to calculate the remaining unknown bankfull dimensions namely average bankfull depth dz bankfull depth dsr and bottom width Ws Using the equations listed below it is possible to calculate the bankfull channel dimensions for any segment over a stream network Manning s equation is commonly used to calculate flow rate and flow velocity for flows as a function of wetted channel dimensions d W Z roughness n and slope So Provided that flow rates are known the wetted channel dimensions are calculated using basic channe
113. culated 9 Topographic Shade degrees Page 151 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 5 5 THERMAL INFRARED RADIOMETRY TIR TEMPERATURE DATA 5 5 1 OVERVIEW OF TIR DATA TIR thermal imagery measures the temperature of the outermost portions of the bodies objects in the image i e ground riparian vegetation stream etc The bodies of interest are opaque to longer wavelengths Atwell et al 1971 On free flowing streams water columns are usually well mixed and surface temperatures represent the temperature of the water column The exception is in thermally stratified areas which may occur in slow deep channels or upstream of impoundments For Oregon DEQ TIR remote sensing a sensor mounted on a helicopter records digital data to an on board computer at a rate that insures the imagery maintains a continuous image overlap of at least 40 The radiometer detects emitted radiation at wavelengths from 8 12 microns long wave and records the level of emitted radiation as a digital image across the full 12 bit dynamic range of the sensor Each image pixel contains a measured value that is directly converted to a temperature Each thermal image has a spatial resolution of less than one half meter per pixel A visible wavelength video sensor captures the same field of view as the TIR sensor Geographic position system GPS time
114. d substances and heat associated with flowing water is called advection Dispersion results from turbulent diffusion that mixes the water column In fact flowing water is usually well mixed vertically largely a result of dispersion Stream water mixing with inflows from surface tributaries and subsurface groundwater sources moves water and heat within the stream system These processes advection dispersion and mixing of surface and subsurface waters redistribute the heat of a stream system via mass transfer Water that is transported by river flow is referred to as advection It follows that advection is a gravity driven process that can only occur in the downstream direction In the case of water temperature no heat energy is lost or gained by the system during advection assuming the heat from mechanical processes such as friction and compression is negligible Advection is simply the rate at which water and the dissolved suspended substances and heat are transferred downstream Dispersion refers to the mixing caused by turbulent diffusion In natural stream systems flows are often vertically mixed due to turbulent diffusion of water molecules Turbulent flows result from a multi dimensional variable flow velocity Page 71 Chapter IIl Dynamic Mass Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 profile with lower velocities occurring near the boundaries of th
115. d an assumed 9 reflection rate applies for diffuse solar radiation Sellers 1965 The portion of solar radiation that is not reflected enters the water column 100 a 2 75 2 Oo FIGURE 2 3 P 5 Calculated Surface 8 3 0 Reflection Reg Values 5S Calculated from Equation N 2 47 25 D T 0 0 20 40 60 80 Solar Altitude degrees Page 46 Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Stream Surface Reflectivity Sellers 1965 If sz gt 80 then TU 0 Rss 0 0515 Os 7 3 638 Elself 0 7 lt 80 then 1 TU Res 0 091 Cos Os mal 0 0386 End If Visual Basic Code 2 47 Direct Beam Solar Radiation Penetrating the Stream Surface Psres P spes 1 Rss 2 48 Direct Beam Solar Radiation Penetrating the Stream Surface Psros P sro 9 91 2 49 Variables Calculated Donp Direct Beam Solar Radiation above Stream Surface m srpa Diffuse Solar Radiation above Stream Surface gt spes Direct Beam Solar Radiation Penetrating Stream Surface Dopps Diffuse Solar Radiation Penetrating Stream Surface Ga Osz Solar Zenith degrees Rss Stream Surface Reflectivity unitless 2 2 80 SOLAR RADIATION HEAT RECEIVED BY WATER COLUMN AND SUBSTRATE Upon penetrating the water surface the portion of the received direct beam solar radiation absorbed by the wa
116. d waves Tidal flows Waves generated by slow control structures sluice gates gates locks etc Chapter III Dynamic Mass Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 3 4 QUANTIFYING EXTERNAL MASS TRANSFERS opague River Multi Spectral Image TEE 1 o T 3 ee r i i E Pi I f Thermal Infrared Image aC are FIGURE 3 7 Example of mixing at a confluence North and South Forks of the Sprague River Oregon 3 4 1 TEMPERATURE CHANGE RESULTING FROM MIXING Receiving water mixing of inflows from surface and subsurface sources will result in the change in temperature and heat as a function of flow volumes and associated water temperatures Such mass transfers occur at specific locations and can have pronounced heating or cooling effects The thermal effect of mixing is more localized and pronounced than temperature changes resulting from heat transfer process The temperature resulting from mixing two volumes or flow rates is easily calculated Resulting Temperature after Complete Mix with Inflow Ty wi Q Tin On 3 32 Q Qn Page 87 Chapter IIl Dynamic Mass Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Variables Calculate Q Flow Rate m Qin m IN Inflow Rate n Tn Inflow Temperature C Tw Water Temp
117. diation Evaporation River KM 279 7 River KM 243 3 Heat Flux J m per sec Heat Flux J m per sec 2 2 2 2 2 2 2 2 2 222 2 2 2 2 2 2 2 2 2 2 22 qiaqaeaqaqaemtioaoaeeadateadadt x lt i lt aqaaeqdaeataedtieaoaeedaeaaadt GOO o Oo Do 6c Oo GO CG So oo o2 Oo OO oO eo Ooo OQ TT SS SS SS SS Se 2 2 2 2 2 2 fe 2 n ANN FTO WOONN YT O ODO ODO NN TO DOONAN YT O HO O FIGURE 2 1 Heat Transfer Terms Grande Ronde River Oregon August 20 1999 Note the variability between sites the temporal variability and the combined effect i e total energy budget term of the five heat transfer mechanisms Page 28 Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 The ultimate source of heat energy to a stream Is solar radiation both diffuse and direct Secondary sources of heat energy include longwave radiation from the atmosphere and near stream vegetation streambed conduction and in some cases groundwater exchange at the water substrate interface Several processes dissipate heat energy at the air water interface namely evaporation convection and back radiation Heat energy is acquired by the stream system when the flux of heat energy entering the stream is greater than the flux of heat energy leaving The net heat energy flux provides the rate at which energy is gained or lost per unit area and is represented as the instantaneous
118. dinal distance Several surface inflows in close proximity creates a possibility that more than one surface inflow is associated with any given model reach over the distance step The methodology accounts for all surface inflows and their associated temperatures and mixes these inflows with the water column Instantaneous Flow Summation of Surface Inflows Qtr pe ed 3 33 Page 92 Chapter Ill Dynamic Mass Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Instantaneous Flow Weighted Temperature of Surface Inflows t t 2 QrriB i t Orie Resulting Temperature after Complete Mix with Surface Inflow rt ue at 4 UM Oe wi 3 35 Qi Qtr Variables Measured Known dx Model Distance Step m Qre Surface Inflow Flow Rate 2 TRIB Surface Inflow Temperature C Calculated Q Flow Rate 2 Qrtrip Instantaneous Flow Summation of Surface Inflows a Ttrigp Instantaneous Flow Weighted Temperature of Surface Inflows C Tw Water Column Temperature C 3 4 4 SUBSURFACE INFLOWS SEEPS SPRINGS AND ACCRETION FLOWS In a similar fashion as used for surface inflows subsurface inflows seeps spring and accretion flows are associated with model reaches The total subsurface inflow rate and the flow volume weighted average temperature are mixed with the model reach water column Instantaneous Summation of S
119. ditions for flow and stream temperature should be entered in columns H gt I Column J represents the cloudiness index the percentage of average daily cloudiness Boundary conditions should consist of measured values Due to the cumulative effects the boundary conditions may seriously alter simulations outputs DELETE CONTINUOUS DATA A message box will ask the user to confirm that they want to delete existing continuous data Configuring the number of continuous data sites data involves changing the entire continuous worksheet If the user can keep track of existing data associations it may be easier to choose not to delete existing data and simple move it appropriately after the continuous data setup configuration If the setup involves significant changes in the number of continuous sites then you may want to delete all of the data and reenter this information Heat Source Continuous Data Setup x x Do you want to clear existing data From the Continuous Data sheet Page 106 Chapter IV Model Operation Page 107 Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Continuous Data Worksheet Rete Window Hei POET or WEN Mon Gm se a UR ee sae 7 Simulation Infermation a 3il Z a Continuous Data Node Locations fot Node t Dena None 1 Data nde Dam Node t Dat Node 2 Daia Node 2 Dat iiaa snirot a Taiji f Trp alte Chin i W
120. dology for the Heat Source Model Version 7 0 Consider a celestial sohere as an imaginary sphere of arbitrary radius upon which celestial bodies in this case Earth may be located the celestial sphere is centered at the observer s position The equation of center of the Sun Oes is calculated as a function of the geometric mean of anomaly of the sun 6 and time measured in Julian centuries t ypc Equation of Center of the Sun degrees cs B 1 914602 t Joc 0 004817 0 000014 type where C 0 019993 0 000101 t jpe D 0 000289 2 11 TU x 5 B sin A C sin B 2 D sin C 3 The true longitude of the Sun 6 is the sum of the geometric mean of the longitude of the Sun 6 and the equation for the center of the Sun Oes True Longitude of the Sun degrees Os Ure T Ocs 2 12 The true longitude of the Sun 6 centered at the Earth is determined by removing any topocentric effects of the observer from the directly observed longitude of the Sun True solar longitude is predicted as a function of time measured in Julian centuries tjpc Apparent Longitude of the Sun degrees Oa 9 5 0 00569 0 00478 sin 25 04 1934 136 tee gt 2 13 Variables Calculated 0 AL lupe Apparent Longitude of the Sun degrees Geometric Mean of Anomaly of the Sun degrees Equation of the Center of the Sun degrees True Longitude of the Sun degrees Geometric Mean of t
121. ds for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Variables Measured Known dx Model Distance Step m dt Model Time Step s g Acceleration of Gravity 9 8 n Manning s Roughness Coefficient S Stream gradient unitless t Time s x Longitudinal Distance m Z Channel Side Slope Ratio dimensionless Calculate A Cross Sectional Wetted Area m dw Average Water Column Depth m Pw Wetted Perimeter m Rp Hydraulic Radius m Q Flow Rate m S Friction Slope unitless U Average Flow Velocity We Bottom Width m Ww Wetted Width m 3 3 3 COMPARISON OF METHODS The Muskingum Cunge method simulates volume storage and dynamic flow routing using a finite difference solution that is based on the continuity and kinematic wave equations There are several methods available for dynamic flow routing each requiring different kinds of data input and each offering varying degrees computational stability and accuracy Of these the Muskingum Cunge method is particularly suited for simulation of hydrodynamics over large and complex stream systems Channel bathymetric data is often unavailable over a large hydrologic scale While such data is required for accurate explicit solutions to complete unsteady hydraulic models the Muskingum Cunge method allows for less bathymetric detail since segment storage is approximated Bedient and Huber 1992 Segment storage and flo
122. e streambed conduction streambed Stream air convection Deonvection and evaporation evaporation Wunderlich 1972 Jobson and Keefer 1979 Beschta and Weatherred 1984 Sinokrot and Stefan 1993 Boyd 1996 Hence the net heat energy flux iota consists of summation of these heat transfer processes With the exception of solar radiation which only delivers heat energy these Air Water convection includes both turbulent and free surface conduction Page 27 Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 processes are capable of both introducing and removing heat from a stream Stream shade is an important regulator of shortwave radiation heat transfer to a stream that can create significant instream temperature increases i e by 1 C or more over spatial scales ranging from a stream segment i e 1 km to the watershed scale Brown 1969 Beschta and Weatherred 1984 Boyd 1996 Heat Transfer Processes oo a a ain Tn i __ D mooo oe Solar Solar Longwave Direct Diffuse Convection Evaporation ff Stream Cross Section Bed Conduction Net Heat Energy Continuity P total solar T P longwave evaporation i convection r streambed 2 1 Heat Transfer Flux Parameters lt Total Energy Budget Alr Convection e Solar Radiation e Bed Conduction e Longwave Ra
123. e Vertical Plane 14 04 F save elt Te it E E 1 Horizontal Plane FIGURE 1 2 Shade geometric relationships and effective shade definition Chapter Introduction Page 14 Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 EFFECTIVE SHADE CASE STUDIES Recent studies have isolated the thermal effects of solar loading and consequently the importance of stream surface shade in moderating localized increases in water temperature Through controlled water bath studies Moore et al 1999 found solar radiation to be a warming influence in both daily maximum and daily minimum water temperatures The study was conducted in varying locations at various elevationsand climatic conditions in Oregon and found similar results at each study site see Figure 1 3 The Effect of Shade on Water A Tub Study J Moore J Miner and R Bower Department of Bioresource Engineering Oregon State University 1999 Two tanks with equal volumes of water and similar initial temperatures were insolated on the sides and bottom One was exposed to August solar radiation while the other was completely shaded Results are presented in the graph below Shaded Tank pon Shaded Tank i Lm pak 5 h pal mk ais ma CL CL CL CL CL CL r r r r r r co 5D mm m m m m m D m m m
124. e polygons as you do the digitizing CODING YOUR RIPARIAN FEATURE POLYGONS There should be one field within your riparian vegetation theme that will contain a numeric code which describes the species canopy density and height of the riparian feature Species Species identification relies on the ground level data and knowledge of the area in which you are mapping vegetation In forested areas you are often only able to distinguish between conifer and deciduous species compositions Therefor an example of species classes to map would be conifer deciduous and mixed conifer deciduous Canopy Density This is an ocular estimate of the canopy closure as observed from the aerial imagery Precise measurements are not possible so it is sufficient to derive classes such as 0 25 25 50 50 75 75 100 Height Since you cannot measure precise stand height from the aerial imagery it is sufficient to derive a few different height classes for your vegetation such as tall medium and short You can eventually apply your ground level data to estimate height ranges or values for these classes The table on the following page lists some example riparian vegetation codes and their corresponding species canopy density and height values The codes may cover narrower ranges of the attributes depending upon the aerial imagery quality experience of the person doing the mapping and amount of ground level data collected Remember These are so
125. e Farm a03 46 OL 0 7 Barren Rock a04 0 0 Uo 0 0 Barren Bank a05 0 0 Oo 0 0 Page 112 Chapter IV Model Operation Page 113 Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 4 3 7 MODEL SETUP MORPHOLOGY DATA DEVELOPMENT OF WIDTH TO DEPTH RATIO INFORMATION The data contained in the Morphology worksheet contain both measured TTools data and assumed or derived values The general procedure for setting up this sheet should start with inserting gradient and banktfull width data from the TTools database The next step is to assign a width to depth ratio W D to each model data node There are two ways to provide the needed W D information The first method and easiest method is to simply insert the W D values directly into the worksheet There is an optional procedure that can be used to associate W D values based on Rosgen level information To associate W D data to a Rosgen stream type press the Enter W D Data button and change the W D data manually Notice that the Rosgen Level Stream Type column is optional This column must be completely filled in with the stream types A gt G before you can proceed after which you can access Associate W D tab in the Main Menu to assign Rosgen based W D values Info General Model Input Model Setup Executables Diagrams Data Sheets Associate W D with Level Rosgen Stream Types
126. e channel i e channel bottom and stream banks Higher velocities occur farthest away from channel boundaries commonly at the top and center of the water column The velocity profile results from the friction between the flowing water and the rough surfaces of the channel Since water is flowing at different rates through the channel cross section turbulence is created and vertical mixing results Dispersion mixes water molecules at a much higher rate than molecular diffusion Turbulent diffusion can be calculated as a function of stream dimensions channel roughness and average flow velocity Dispersion occurs in both the upstream and downstream directions Advection Dispersion Tributaries Groundwater Downstream Turbulent Mixing with Mixing with transport mixing other subsurface associated associated surface flows with flowing with flowing flows water water Hyporheic Flows Channel Bottom FIGURE 3 1 Mass Transfer Processes Advection Dispersion and Mixing Lateral Velocity Distribution Vertical Velocity Distribution Channel Edge Left Bank Water Surface Channel Edge Right Bank Channel Bottom FIGURE 3 2 Dispersion Defined Dispersion is the mixing that occurs from turbulence caused by vertical and lateral flow variations Velocity is a function of depth width and channel roughness frictional forces at the boundaries The vertical and horizontal gradient in flow velocity causes tumbling and eddy effe
127. e difference forms with respect to distance 1 and time t These forms are then substituted into the two governing Page 81 Chapter III Dynamic Mass Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 equations and rearranged to solve for the central difference parameter in time t The time step dt must be small relative to the distance step dx to calculate an accurate approximate The stability conditions listed in 8 30 and 8 31 will ensure that this assumption is correct and prevent numeric instability and minimize numerical diffusion The smaller of the two time step values should be used THE COMPUTATIONAL PROCEDURE CONSISTS OF THE FOLLOWING STEPS 1 Determine stability condition for each distance step i for the time step t using the Courant 3 30 and friction stability equations 3 31 For each time t calculate the smallest dt value for all segments i 2 Solve for dy using the finite difference form of the continuity equation 3 26 3 Calculate the friction slope s from equation 3 28 4 Solve for U using the finite difference form of the conservation of momentum equation 3 29 5 Calculate Qt as a function of dy and U Finite Difference Form of the Derivatives aU _ Uia Ui au Ut u Ox 2 dx ot dt dw _ dwin dwin dw _ dwi dwi Ox 2 dx ot dt Substitution into the Continuity Equation 3 13 yie
128. e the finite difference time steps while ensuring numeric stability however there are other forms of instability with this approximation method This explicit approximation is completely physically based and therefore highly Page 76 Chapter IIl Dynamic Mass Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 sensitive to bathometric data It is fundamentally important that the quality and Spatial resolution of bathometric data is excellent Other forms of instability may result from rapidly varied flows event driven highly managed major mass transfers which bolsters the concern of the suitability of this numerical solution technique The overall performance of each method will vary based on the application Both methods are included in the model because strong cases can be made for the selection of one method over the other based on the spatial scale of model application the complexity of system hydrodynamics and data availability ST VENANT GOVERNING EQUATIONS Continuity Equation form 1 Bedient and Huber 1992 dS dt i i 1 Continuity Equation form 2 Bedient and Huber 1992 Oa Uy Ow ot OX OX Momentum Equation Bedient and Huber 1992 aU aU dw iN Y Dae a LE o S 3 14 z U a g So oy 3 14 0 3 13 Flows Assumed to be Unsteady and Varied Non Uniform 0 N29 Menand eo Lap 3 15 ot ot OX OX Variables Meas
129. e uncorrected for refraction Page 36 Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Refraction Correction Coefficient Cp If a gt 85 then Cp 0 If 5 gt a lt 85 then 58 1 0 07 0 000086 3 5 180 a a a 180 180 180 aam e A 180 A 3600 If 0 575 gt a lt 5 then _ 1735 a 518 2 a 103 4 a 12 79 a 0 711 C 3600 If a lt 0 575 then Ce 20 74 Tarf o k 3800 180 2 24 0 5 8 O 0 4 G o o Q 0 3 FIGURE 2 2 5 3 Calculated Refraction o 0 2 Correction Coefficient Cp E Values Based in Equation 2 Q 0 1 24 lt 00 0 20 40 60 80 Solar Altitude degrees Solar azimuth is the angular distance measured clockwise along the horizon from a specified location stream segment to the intersection with the great circle drawn from the zenith through a body on the celestial sohere The solar azimuth comprises the horizontal position of the sun relative to the stream segment Solar Azimuth lbgal 1983 0 gt 7 lt 360 SiO as cod osz i s k _ 180 i 180 i 180 2 25 C68 bne Sin Gao Ou osz Z Taken from NOAA Surface Radiation Branch http www srrb noaa gov highlights sunrise azel html Page 37 Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Ma
130. each land cover zone m SLic Shadow Length Cast from each Zone m 2 2 60 SOLAR RADIATION HEAT ABOVE STREAM SURFACE To account for shade cast from a stream bank or a near stream topographic feature the shadow length SLsg originating from topography on the appropriate stream bank is calculated for each of the land cover zones If the bank is shading the stream surface then the direct beam flux is completely attenuated Direct Beam Solar Radiation below Stream Banks For Zone 4 To 1 Step 1 SL og Zone eine TU tan Oa me aa If SLop Zone gt Wc Zone Zone then Psrg4 0 Else P sRB4 z D spp3 End If Next Zone Visual Basic Code 2 43 Diffuse Solar Radiation below Stream Banks P srD4 Vsrpv3 2 44 Page 44 Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 lf there are types of emergent vegetation vegetation growing in the water column and emerging over the stream surface then shading from this vegetation is also calculated as a function of path length PL c and vegetation density VD Direct Beam Solar Radiation below Emergent Vegetation Plic 0 al 0 SIN Dea z sp 180 If PL 0 gt Wy then PL 0 Wy io 0 1 Exp 20 VPO py 0 gpp4 Pgapa 1 Yc 0 Visual Basic Code 2 45 Diffuse Solar Radiation below Emergent Vegetation Plic 0 Hlc 0 Kol0 1
131. ed Known C Cloudiness unitless H Humidity unitless o Stefan Boltzmann Constant 0 0000000567 Ta Air Temperature C Tw Water Temperature C Calculated Eatm Emissivity of the Atmosphere unitless ea Vapor Pressure mbar es Saturation Vapor Pressure mbar Piongwave Water Column Received Longwave Radiation Flux P Atmospheric Emitted Longwave Radiation Flux pt Land Cover Emitted Longwave Radiation Flux 3 A Sy Water Column Emitted Longwave Radiation Flux 3 m Oyrs View to Sky unitless Page 52 Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 2 3 SUBSTRATE CONDUCTION FLUX P onpuction Ea ae a y He eas i 5 aT Heat exchange between alluvium and the water column acts as a heat buffer with the stream and does so as a function of particle size embeddedness and channel geometry Heat energy conduction between the stream bed and the water column is driven by a heat gradient and is rate limited by the size and conductance properties of the substrate Conduction transfers heat to the stream during periods of the day when thermal differences between the substrate and water column are most pronounced The effects of conduction can vary greatly Heat transfer to the water column from conduction typically broadens the diel temperature profile rather than increasing the
132. ediately Returned to Water Column as Heat B4 B3 0 53 1 n 2 68 Diffuse Solar Radiation Flux Reflected from Stream Bed B5 B2 Rez 2 69 Diffuse Solar Radiation Flux Attenuated from Stream Bed to Surface B6 BS 1 TD 2 70 Diffuse Solar Radiation Flux Attenuated in Water Column sppe B1 B4 B6 2 71 Diffuse Solar Radiation Flux Attenuated in Stream Bed Page 49 Chapter Il Heat Transfer Page 50 Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Variables Measured Known n Porosity of the Stream Bed unitless Calculated dw Average Water Column Depth m ls sprgs Direct Beam Solar Radiation Penetrating Stream Surface m sprps Diffuse Beam Solar Radiation Penetrating Stream Surface a sprge Direct Beam Solar Radiation Attenuated in Water Column 4 m srp Diffuse Solar Radiation Attenuated in Water Column m sre Solar Radiation Attenuated in Water Column m oa Solar Radiation Attenuated in Water Column 4 m srez Direct Beam Solar Radiation Attenuated in Stream Bed 4 m sprpz Diffuse Solar Radiation Attenuated in Stream Bed m Mon7 Solar Radiation Attenuated in Stream Bed ea Osa Solar Altitude degrees Osz Solar Zenith degrees Res Reflectivity of Stream Bed if Direct Beam Radiation unitless Res Reflectivity of Stream Bed if Diffuse Radiation unitless T
133. efficient Apparent Longitude of the Sun degrees Geometric Mean of Anomaly of the Sun degrees Solar Azimuth degrees Equation of the Center of the Sun degrees Hour Angle degrees True Longitude of the Sun degrees Geometric Mean of the Longitude of the Sun degrees Mean Obliquity of the Elliptic degrees Obliquity of the Elliptic degrees Solar Altitude degrees Solar Zenith Uncorrected degrees Solar Zenith Corrected degrees Solar True Anomaly degrees Topographic Shade Angle West degrees Topographic Shade Angle South degrees Symbols Analytical Methods for Dynamic Open Channel Heat and Mass Transfer SYMBOLS O7_ E Ovts ae P Pw PLic PLy Slic Sits Sot Ta typ tpc tpst temr Le lt tone Tow Page 186 TRIB Tw Methodology for the Heat Source Model Version 7 0 Topographic Shade Angle East degrees View to Sky unitless Adiabatic Atmospheric Pressure mb Solar Radius Vector AU Wetted Perimeter m Direct Beam Path Length through each land cover zone m Direct Beam Path Length through Water Column m Flow Rate m Evaporation Loss Rate Surface Inflow Flow Rate Subsurface Inflow Rate m Hyporheic Exchange Rate Across Seepage Face Surface Inflow Rate m Withdrawal Flow Rate m Instantaneous Flow Summation of Surface Inflows m2 Withdrawal Flow Rate x Stream Surface
134. el Since this model is shareware we invite user suggestions for improvements in methodology and coding The collective intuition of the modeling community can contribute to the refinement of these and related analytical methods Please let us know what improvements or changes you have made or are considering our contact information is listed on the cover page The Heat Source methodology is unique and will prove to be a different modeling experience especially to the uninitiated Microsoft Excel is used to store and configure the model inputs and chart store the model outputs Visual Basic programming is utilized from all of the model functions model setup executables and data formatting The Main Menu can be accessed from all of the worksheets except those containing charts and contains all of the model functions as well as the fundamental general inputs This model format has been selected for the ease of model design programming and the widespread availability of Excel The large quantity of input and output data required for Heat Source modeling is easily handled by using multiple worksheets in Excel for storage No calculations are performed within the spreadsheets to minimize model size and maximize computational efficiency Further cell formatting is minimized due to Excel s tendency to count formatted cells as occupied and greatly increase the Excel file size a phenomenon widely known as spreadsheet bloat The only way to remo
135. emporal scales Tremendous spatial variability occurs across a watershed and is compounded Page 5 Chapter Introduction Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 by adding the temporal component At any stream reach thermal processes constantly change throughout the day month and year Stream temperatures are a result of a multitude of heat transfer and mass transfer process The conceptual and analytical challenge is to develop a framework that captures these forms of variability to the best possible extent while constantly investigating potential analytical improvements The recognition of limitations such as those presented by microclimates is important for several reasons While these limitations outline potential areas of weakness in the methodology presented in this document acknowledgement of data and methodology weaknesses makes it possible to undertake a comprehensive approach define the limitations maintain credibility and identify future research needs Acknowledgement of the limitations is in accordance with the scientific method and recognizes that analytical efforts should provide a rigorous comprehensive statistically valid and advanced treatment of stream temperature dynamics 1 1 2 ACKNOWLEDGEMENT OF LIMITATIONS Capturing and understanding the thermally important parameter variation across a complex landscape coupled with quantifying hydro
136. endar Every year that is exactly divisible by four is a leap year except for centurial years which instead must be divisible by 400 to be leap years By this definition the year 2000 is a leap year Daylight Savings Corrected Time t t hours 2 2 DST 24 2 2 Greenwich mean time is the corresponding time in Greenwich England calculated as a function of daylight savings time and the time zone correction factor Greenwich Mean Time t t ft gp e 9 3 GMT DST 24 hours Table 2 1 Time Zone Correction and Meridian as a Function of Time Zone United States Time Time Zone Correction Zone Name Factor tone Central Meridian East 5 hours 75 Central 6 hours 90 Mountain 7 hours 105 Pacific 8 hours 120 The Julian day is commonly used to calculate solar parameters as a continuous numeric expression of calendar day The Julian ephemeris date is then converted in Julian centuries units of 36525 ephemeris days from the epoch 1900 January 0 5 ET Julian centuries are calculated since epoch 1900 January 0 5 ET this time variable will be used heavily in calculating the earth s position Julian Day typ INT 365 25 Y 4716 INT 30 6001 M 1 D B 1524 5 2 4 United States Government Printing Office The Astronomical Almanac for the Year 1998 Washington DC Navy Dept Naval Observatory Nautical Almanac Office If the date is between the first Sunday in April and the last Sunday in Oct
137. ent of your digitized stream theme and B You use the Show Loose Ends tool to identify overshoots undershoots and C There are no red dots within your stream polyline only one on each terminal end Page 163 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 5 7 4 UNIONIZING THE CLEANED STREAM POLYLINE Once you have cleaned your digitized stream polyline of all undershoots overshoots you must unionize the records within the table This process essentially takes multiple segments that comprise your stream layer and melts them into one single continuous line i e it converts a multi record database table into a single record database table T Tools only works ona unionized line theme 1 Open the TTools menu and select the Unionize Polyline option 2 Name the new file this will be your cleaned and unionized stream polyline that TTools sampling will be based from Helpful Hint It is a good idea to use a naming convention like ColdCreek_clean_utm This file name includes the stream name identifies it as cleaned and indicates the projection 3 Now open the Table of your new theme and make sure that it consists of only one single record If there are multiple records there is an error in your stream polyline and you must repeat the cleaning process to check for missed overshoots or undershoots Page 16
138. er 69 364 Marciano J J and G E Harbeck 1952 Mass transfer studies in water loss investigations Lake Hefner studies USGS Prof Paper 269 Martin J L and McCutcheon S C 1999 Hydrodynamics and Transport for Water Quality Modeling Lewis Publishers New York NY 1999 McCutcheon S C 1989 Water Quality Modeling Vol 1 Transport and Surface Exchange in Rivers CRC Press Boca Raton pp 183 209 Meeus J 1988 Astronomical Formulae for Calculators 4 Ed Richmond Virginia Willmann Bell Inc Meeus J 1991 Astronomical Algorithms 2 Ed Richmond Virginia Willmann Bell Inc Page 191 References Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Meyer A F 1928 Elements of hydrology 2d ed revised New York John Wiley amp sons 522 p Meyer A F 1942 Evaporation from lakes and reservoirs Minnesota Resources Commission St Paul MN Moore J Miner J and R Bower 1999 The effect of shade on water a tub study Department of Rangeland Resources Oregon State University Morton F I 1965 Potential evaporation and river basin evaporation J Hydraul Dive Prac Am Soc Civ Eng 91 HY96 67 97 National Oceanic and Atmospheric Administration Surface Radiation Branch Solar position calculator website http Awww srro noaa gov highlights sunrise azel html Norton W R L A Roesner and G T Orlob 1968 Mathematical models for
139. erature C 2 C A woe 0 gs 1 S F grow PO WEE g i 5 5 oc FIGURE 3 8 Inflow Receiving Temperature Changes that Accompany Mixing fifo E A naan Rh it Om B95 are 2 C 32 32 32 32 32 rat D R Ratio of Inflow to Receiveing Flow Rates 3 4 2 THERMAL INFRARED RADIOMETRY DERIVED MASS BALANCE APPROACH Remote sensing using thermal infrared radiometry TIR can easily identify areas where heat change occurs due to mixing with surface and subsurface waters All water temperatures are apparent in TIR sampled stream temperature data and provided that at least one instream flow rate is known the other flow rates can be calculated In this fashion TIR sampled stream temperature data can be used to develop a mass balance for stream flow using minimal ground level data collection points Simply identifying mass transfer areas is an important step in quantifying heat transfer within a stream network For example using TIR data thirty one discrete mass transfer processes were located and quantified in the North Fork Sprague River Oregon Boyd and Kasper 2002 Several of the subsurface mass transfer areas were unmapped and the relative thermal and hydrologic impact to the stream system was not previously quantified Further surface returns from agriculture irrigation were previously unmapped and consequently were not quantified in terms of flow rates or temperatures Page 88 Chapter Ill Dynamic
140. erature patterns The reasons for these thermal differences are found in the cumulative effects of highly variable characteristics of the land cover morphology mass transfer inflow and withdrawal distributions Boyd and Kasper 2002 TTools sampling Tool samples spatial data sets such as stream position elevation gradient channel width topographic shade and land cover types from GIS data at user defined intervals This documentation is developed to support TTools version 7 0 Page 2 Chapter Introduction Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 South Fork North Fork 16 04 16 31 August 12 1999 TIR Measured Stream Temperature C FIGURE 1 1 TIR Sampled Stream 16 20 16 44 August 16 1999 Temperature Patterns for the North and South Fork Sprague River Stream Kilometer How DOES HEAT SOURCE ADDRESS THESE UNIQUE THERMAL PATTERNS With recognition of the unique thermal dynamics of streams and rivers comes the need for an analytical framework that accommodates the variability and Spatial distributions inherent to land cover morphology and hydrology The past ten years have brought about increased use of remote sensing computational power and ease of programming ground level data collection methods and other improvements that are all part of the basis for proposing an improved stream temperature analytical framework Analytical
141. es relative to deep cold subsurface sources of flow As with any generalization there are exceptions And no generalizations Page 21 Chapter Introduction Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 can be made when considering the effects of surface inflows and confluences since each stream system and waterbody has a unique thermal behavior To the extent that tributaries and subsurface flows are unaffected by human activities an argument can be made that changes from some mass transfers reflect background conditions rare Thermal Infrared Over Multi Spectral Image Multi Spectral Image q E i z J Thermal Infrared Color Map l I i a it iec FIGURE 1 7 Subsurface inflows can significantly cool streams and rivers Page 22 Chapter Introduction Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 1 3 MODEL APPLICATION SCOPE SCALE amp CUMULATIVE EFFECTS Cumulative effects are those effects on the environment that result from the incremental effect of the action when added to past present and reasonably foreseeable future actions Cumulative effects can result from individually minor but collectively significant actions taking place over a period of time Forest Ecosystem Management An Ecological Economic and Social Assessment Report of t
142. etry data Calibrated with unfamiliar with the BankFull Morph Manning s roughness coefficient methodology Evaporation Hydraulic Madels Flow Routing Explicit Finite Difference Method Elestr Seeks Calculate Muskingum Storage Factor X Required for Heat Source and Flow Router Aporaonate model use soe smear iis Ol at and apohcation are the Cii sole responsibilty ofthe Tre e USEF Environmental Department of gt Lali ree a j T i i 7 i S 2 DIX i i Sa come gl Hide Main Menu i Page 120 Chapter IV Model Operation Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 4 3 11 MODEL SETUP CLEAR ALL DATA SHEETS This model function will clear all of data in all of the worksheets in the model Use this function when you want to start over or create a new model Be careful Important Info General Model Input Model Setup Executables Diagrams Be Careful Data Sheets Clear All Data Sheets Continuous Data This will clear all of the input and output data in all worksheets Mass Transfer Data Vegematic Associate w D Bankfull Morph Evaporation P This should be used when you Clear All Data Flow Routing want to remove all ofthe data in Sheets all of the sheets Asoraonate model use and anoication are the sole responsibilty of fhe user ia a Department of ah zas Tad roe Environmental n E
143. ey shape landform and topographic shade angles 5 4 1 STREAM ELEVATION Stream elevation is measured from a DEM TTools will auto detect the pixel size either 10 meter or 30 meter of the DEM In order to find the lowest pixel nearest to the stream segment node T Tools samples 25 pixels the pixel that falls directly on the stream segment node and two pixels in each direction Surrounding it The lowest elevation sampled is assigned to the stream segment node FIGURE 5 10 The procedure for sampling stream elevation involves twenty five discrete samples in a radial pattern to locate the lowest datum Page 149 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 5 4 2 STREAM GRADIENT Stream gradient is calculated from the elevation of the stream node and the distance between nodes The DEMs have a 3 3 feet one meter elevation resolution It commonly occurs that a measurable i e greater than 3 3 feet elevation drop spans several of the stream segment nodes Gradients are calculated as Stream Gradient Calculation i Zi So 5 1 oer ek 5 1 Variables Measured Known dx Distance Step m i Stream Data Node i Last Stream Node Where Zp gt z Z Elevation s Calculated S Stream Gradient unitless 5 4 3 TOPOGRAPHIC SHADE ANGLE The maximum topographic shade angle is calculated to the east south
144. f your T Tools point theme you may get a message that says Spatial Analyst has reached its sampling capacity Click OK and TTools will automatically save your project and close your ArcView session At this point re open your ArcView project and start the Sample Vegetation Grid process again This time DO NOT overwrite existing values and T Tools will begin sampling where it left off last time 8 Repeat this process as many times as necessary until you see a window pop up that says Riparian land cover has been sampled Page 180 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 STEP 6 SAMPLE FLIR DATA PREREQUISITES e You must have your TTools point theme in the view e You must have your FLIR point theme in the view STEPS 1 Select the Sample FLIR Data option in the TTools menu 2 Select your TTools point theme 3 Select the FLIR point coverage that you will be sampling 4 Select the field from your FLIR point theme that contains the temperature values you wish to sample Typically the Median field is sampled from Watershed Sciences LLC data sources 5 Select the temperature units that exist in the FLIR point coverage Page 181 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer SYMBOLS C C Cpr CoL
145. fer Methodology for the Heat Source Model Version 7 0 4 4 2 EXECUTABLES FLOW ROUTER Flow Router is the hydraulic flow routing model either Muskingum Cunge or Explicit Finite Difference Method eApplication Simulate dynamic flow routing wetted channel dimensions and Info General Model Input Model Setup Executables Diagrams Shade a lator Calculate Open Channel Hydraulics pues hydraulics includin Flow Router select to Flow Router to calculate open channel wetted T cluding Heat Source deminsions hydraulics and to route stream flow throughout the yporheic flows channel network Inputs All Calculations use the Muskingum Cunge Method or the Explicit Hear cone Method selected under the Model Setup and Flow Routing tne Morphology Data tabs See model documentation for a description of each worksheet Flow Data method worksheet and Flow a Boundary Conditions Flow Router uses inputs from the In the Continuous Morphology Data and Flow Data Data worksheet If worksheets 7 evaporation losses are included all of the input sheets should be i 7 er completed ppropriate model use 5 Rur anp and application are the Outputs Output oe M Gigni sole responsibility of the Hydraulics Oregon a USEF Department of Ours Environmental i a rs Hide Main Menu ii ane at Page 125 Chapter IV Model Operation Analytical Methods for Dyna
146. fer Methodology for the Heat Source Model Version 7 0 Relationships Between Effective Shade Near Stream Vegetation and Channel Morphology Effective Shade is a Function of Two Interrelated Parameters Land Cover and Morphology Stream surface shade isthe primary control over the daytime rate of stream heating from direct beam solar radiation Simply put shade is a dominant control over the rate of stream heating e ae gt et Near Stream vegetation controls shadow length and therefore the timing of stream surface shade amp E k E 7 A L mi E a Ta a rr T i i ta p J m E n j Y _ os a Er zr i F m Tai j Trout Gr Near stream vegetation and channel morphology conditions are highly interrelated since each affects the condition of the other E Te FE E Pie pak bes E a ey ms im k ie a Seater pi Foal Fare er SS Channel morphology determines S23 the shadow length necessary to 5 shade stream In effect channel morphology controls the size of the stream surface area oe S Cr Eri SH gr ta a Channel morphology condition and hear stream vegetation combine to control the amount of stream surface shade shade that occurs on any given stream segment Swe La P i a uf i a e Fite ee a Page 12 Chapter Introduction Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0
147. fer Methodology for the Heat Source Model Version 7 0 Table 1 2 Modes of Thermally Induced Cold Water Fish Mortality Brett 1952 Bell 1986 Hokanson et al 1977 Modes of Thermally Induced Fish Mortality Instantaneous Lethal Limit Denaturing of bodily enzyme systems Incipient Lethal Limit Breakdown of physiological regulation of vital bodily processes namely respiration and circulation Sub Lethal Limit Conditions that cause decreased or lack of metabolic energy for feeding growth or reproductive behavior encourage increased exposure to pathogens decreased food supply and increased competition from warm water tolerant species Temperature Time to Range Death gt 90 F Instantaneous 2092C 72 F 77 F 220C 25 C Hours to Days 64 F 72 F Weeks to 17 8 C 22 C Months Chapter Introduction Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Chapter Heat Transfer Description of Processes Analytical Methods and Finite Difference Approximation The ultimate source of terrestrial and atmospheric heat energy is solar radiation images from SOHO telescope and Apollo 17 mission 2 1 OVERVIEW Stream temperature change is an expression of heat exchange between a stream and its environment The heat transfer processes that control stream temperature include solar radiation soiar longwave thermal radiation Diongwav
148. fforts to obtain remotely sensed TIR data In fact TIR data alone usually proves to be more informative than any modeling effort in assessing the current spatial distribution of stream temperatures and should be a primary focus stream temperature assessments TTools should be used to associate TIR sampled temperature data with individual stream data nodes These data can then be directly entered into column U from the TTools database Important Pay particular attention to entering exact times for sampling over the stream length Heat Source will match the closest simulated values both temporal and spatial the time and location represented by the TIR data points A statistical comparison between simulated values and TIR data is provided as model output CONTROLLED FLOW TEMPERATURE AND DEPTH DATA Most stream and river systems have control structures where hydraulics are subjected to natural or more commonly human controls such as reservoirs weirs check dams diversion structures etc The user has the ability to add these features to the instream hydraulics and flow routing routines where they cannot be calculated from traditional gravity and friction based methods Where data are entered these values become fixed flows temperatures and depths For example behind a bottom release dam there will be a controlled flow that has a fairly constant temperature and likely a constant wetted depth In this case it would be appropriate to add t
149. gal math function i e the arctangent of zero square root of a negative number etc or with illegal code syntax i e open loops and logic statements Unless triggered by the user this message signifies serious problems with either the code or the input data that cannot be resolved without changes that address the underlying problem s Microsoft isual Basic f i Code execution has been interrupted Continue ERROR MESSAGES There are embedded in the code several error messages that will notify the user that a problem has occurred All of these error messages terminate with an end to the model run Examples of such error message boxes are presented below Heat Source Flow Router x amp Missing data Flow Router Terminated Heat Source FUBAR l xj x Slope cannot be less than or egual to zero unless you enter 4 control depth Page 135 Chapter IV Model Operation Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Heat Source Finite Difference Grid Is Unstable E xX x Hydraulics are unstable For this Finite element the time step should be less than 2 minutes Heat Source Flow Router i x x Missing flow boundary condition For day 0 Itis likely that you have changed the simulation period and need to completely enter the continuous and Flow data inputs Heat Source Simulation x x Model is unstable
150. ght area with three to six in situ measurements per survey Weather conditions including sky conditions air temperature and relative humidity are collected for the times of the survey at fixed weather stations e g USFS remote automated weather stations RAWS Agrimet local airports or using portable weather stations The recorded TIR images contain measured radiance values that are then converted to surface temperatures based on the calibration factor of the sensor emissivity of natural Page 152 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 water atmospheric transmission and ambient reflections multi scattering For the calculations the emissivity of the stream is assumed to be 0 96 which is the within the 0 92 to 0 96 range published for natural water Avery and Berlin 1992 This assumption is made while also recognizing that slight changes in emissivity result from differences in surface roughness Torgersen et al 2001 and Suspended sediments Wen Yao et al 1987 The error contribution from these factors in TIR derived stream temperature measurement is quite small i e less than 0 5 C The atmospheric transmission of the emitted energy between the water surface and the sensor is simulated with the MODTRAN atmospheric transmission model and using the measured weather conditions at the time of the survey Berk et al 198
151. h ANGAS Pipe Quality Hide Main Menu m The user is prompted before the model deletes all of the data from all worksheets This process cannot be undone Heat Source Clear Data x x Do you want to clear existing data From all worksheets al Page 121 Chapter IV Model Operation Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 4 3 12 MODEL SETUP VALIDATION DATA Hydraulic and shade information can be entered in to the Validation Data worksheet and the model will pair simulated values to the location and date of the measured values Flow rate velocity and wetted channel dimensions will be paired with measured data at the completion of a simulation Validation Data Worksheet Measured Data Locational Average Max Information Stream Flow Velocity Wetted Wetted Wetted optional Date km cms ims Width mj Depth mj Depth m u s French Camp 871971999 33 10 1 57 U2 19 81 0 25 0 64 Lake Cr CG 8719 1955 24 00 2 35 0 35 14 335 0 33 0 67 st bridge 8719 1955 21 10 3 10 0 61 4 14 O42 0 76 Gage atBakerAd 6 23 1999 4 00 1 42 Gage atBakerAd 6 25 1999 1 60 2 12 DEQ mouth of 19 1999 0 25 2r9 0 58 11 83 0 26 0 49 Simulated Data Average Max Measured and simulated data ele ete Oe ERa neet pe cms ims Width m Depth mj Depth mj are paired for validation E aA 110 IE neo 1 50 0 36 12 60 0 24 0 43 2 04 0 36 13 10 0
152. hange is inversely proportional to flow volume A method is developed in Heat Source that allows flow volumes to reach zero without model failure i e division by zero errors Heat Source will notify the user once stream flows have reached 1 4 cfs 0 0071 cms or less and will ask whether the operator would like to continue This message is basically asking the user whether the low flows being simulated reflect the true condition At this time the model operator can either stop the model run or continue the simulation The model will not ask the user again about encountered flow volumes for the duration of the simulation Once a user selects to continue the simulation the model simply skips the stream nodes without sufficient flows to route i e less than 1 4 cfs In these stream nodes hydrologic and heat processes are not calculated and output variables are assumed to be zero Proceeding downstream the model will detect when flows become sufficient to commence flow routing again i e greater than 1 4 cfs Of particular concern is the estimation of the water temperature in this first stream node below the dewatered section where flows are sufficient for flow routing and heat transfer modeling In essence this stream node represents a boundary condition The model estimates this stream node temperature as the last known stream temperature value in the closest proximity to the stream node It is likely that this assumption will be mini
153. he Forest Ecosystem Management Assessment Team Analytical methods listed in this paper allow dynamic simulation of both heat and mass transfer Applications include open channel flows distributed stream networks wetlands and large rivers systems An obvious limitation is one dimensional flow routing This methodology does not include vertical temperature variations but instead simulates an average water column temperature This methodology is intended to simulate variable longitudinal temperature gradients and temporal rate changes as a function of physically based formulae to meet regulatory agency and academic modeling needs As with any analytical model the application including spatial and temporal scales is determined at the discretion of the user largely as a function of the model application Stream temperature changes result from upstream and local conditions Incremental increases can combine to create relatively warm stream temperatures Water has a relatively high heat capacity Cp 10 cal kg K Satterlund and Adams 1992 Conceptually water is a heat sink Heat energy that is gained by the stream is retained and only slowly released back to the surrounding environment Any given measurement of stream temperature is the result of a multitude of processes occurring upstream as well as those processes acting at the site of measurement For this reason it is important to consider stream temperature at a stream network scale
154. he Longitude of the Sun degrees Julian centuries since epoch 1900 January 0 5 ET The angular distance on the celestial sohere north or south of the celestial equator is measured along the hour circle passing through the celestial object Declination is usually given in combination with right ascension or hour angle and can be visualized as the latitude at which the sun is directly overhead Dingman 2002 The earth tilts on its axis causing the solar declination to vary regularly Page 33 Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 between 23 5 and 23 5 Solar declination 8 is calculated as a function of the obliquity of the elliptic 65 and the apparent longitude of the sun 6 Solar Declination degrees eee T l T 180 The true anomaly of the Sun 8s is the sum of the geometric mean of the longitude of the Sun 6 and the equation for the center of the Sun cs Solar True Anomaly degrees Orn One Oces 2 15 The distance to the sun or radius vector P is a function of eccentricity of the Earth s Orbit Eo and the true anomaly of the Sun 8s and is measured in AU units Solar Radius Vector 2 oe 1 000001018 i Ec 2 16 1 Ec Cos Ora The Equation of time E is the hour angle of the true position of the sun minus the hour angle of the fictitious mean posit
155. he Muskingum Cunge finite difference solution used to simulate dynamic flow routing It is important to consider that the calculation of wetted channel dimensions dw Ww Ax Pw Rn and Manning s velocity U at each distance and time steps is necessary for this method Where these terms are listed such calculations are performed as a function of constant and known parameters Wer Ws der Z So and flow rate Q The procedure for approximating the Muskingum Cunge finite approximation follows a three point scheme The derivation of the partial derivatives relies ona three point finite difference form largely taken from Bedient and Huber 1992 n Wedge Storage AKA Q Qi 4 FIGURE 3 4 Muskingum Cunge Wedge and Prism Storage Recall the Continuity Equation Form 1 3 12 B A An di Volume Storage S Bedient and Huber 1992 S K Qiy K X Q Qi 3 16 Page 78 Chapter IIl Dynamic Mass Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Change in Flow AQ with Respect to Stream Segment Cunge 1969 AQ Q Q K S X Q 1 X Qa 3 17 Finite Difference Form of 3 17 Bedient and Huber 1992 lt kan 1 X Qi xaj 1 ah Zo ak 0 alu 3 18 It can be shown that when K dx c that equation 3 18 is the finite difference form of the kinematic wave equation 38 19 provided that ck dQ dA and diffusion is included Bed
156. he bank line away from the stream line Thus TTools will report values of ZERO in the channel width column for such locations It is your responsibility to manually insert field measured NSDZ values into the TTools database file STEP 3 MEASURING STREAM ELEVATION AND GRADIENT This procedure uses Spatial Analyst to sample a grid theme Spatial Analyst can perform a limited number of commands about 32 000 in a given ArcView session before causing a Segmentation Violation and crashing ArcView Therefor it is strongly recommended that you save the project completely close out of ArcView and re open the project before beginning this step of TTools Doing so will clear ArcView and Spatial Analyst memory and TTools will then be able to accurately predict and prevent a potentially disastrous crash Page 177 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 PREREQUISITES e You must have your TTools point theme in the view e You must have a 10 meter or 30 meter DEM in the view The DEM must have been mosaiced and must extend at least nine miles around the stream that is being sampled Helpful Hint Before proceeding with TTools sampling make sure that your DEM and TTools point coverage are located on your local hard drive If your DEM resides on a network drive TTools sampling will take about three times longer STEPS
157. hese data to override the other hydraulic Page 117 Chapter IV Model Operation Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 data calculated in the tradition flow routing methods Any one of these control parameters flow temperature depth can be added without the others Further any combination can be used as long as values are realistic and appropriate Using these control parameters allows the model to simulate through a reservoir or other control structure without introducing model error in the heat or mass transfer methods Morphology Data Worksheet Controlled Flows Depths and Temperatures yn See Important Optional 0 Signifies no data Zero or null values Controlled Controlled indicates that no TIR TIR Temps Controlled Depth Temperature Control flows Date Time CC Flows cms m o temperatures or depths are occurring at the corresponding data node 4 3 8 MODEL SETUP EVAPORATION RATE METHODS Heat Source allows the user to select the evaporation rate method as either the mass transfer method or the combination method Penman Fora comprehensive review of these methods see Section 2 4 1 Evaporation Rate Both methods rely on a wind function that utilizes coefficients a and b See Table 2 3 Wind Function Coefficients for appropriate a and b values Values for these coefficients can be either inpu
158. iability USFS Remote Sensing Applications Center Salt Lake City Utah Fisher H B E J List R C Koh J Imberger and N H Brooks 1979 Mixing in Inland and Coastal Waters Academic Press New York 1979 Hall F C 1998 Pacific Northwest Ecoclass Codes for Seral and Potential Natural Communities USDA Forest Service Pacific Northwest Research Station PNW GTR 418 Harbeck G E and J S Meyers 1970 Present day evaporation measurement techniques J Hydraulic Division A S C E Prceed Paper 7388 Harbeck G E Kohler M A Koberg G E and others 1958 Water Loss Investigations Lake Mead Studies USGS Prof Pap 298 100 p Page 190 References Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Heath A G and G M Hughes 1973 Cardiovascular and respiratory changes during heat stress in rainbow trout Salmo gairneri J Exp Biol 59 323 338 Hogan J W 1970 Water temperature as a source of variation in specific activity of brain acetylcholinesterase of bluegills Bull Environment Contam Toxicol 5 347 353 Hokanson K C F Kleiner and T W Thorslund 1977 Effects of Constant Temperatures and Diel Temperature Fluctuations on Specific Growth and Mortality Rates and Yield of Juvenile Rainbow Trout Salmo gairdneri J Fish Res Bd Can 34 639 648 Ibqal M 1983 An Introduction to Solar Radiation Academic Press New York 213 Pp I
159. ich oe 1063 ozs 5259 DHANNS SINS ees Hoa HY Morphology byes yf Continuous pata pioa pate veldanon bate 2 chattel temo f Chat Tik ff Chettong Temp if Chort solar Fin j phates Fin ff chatchede fla Tl Dues Ce Apo 3 COORD Jo S 4 A Sr gt eE Be bw Seuuty P E oo Reade WH Heat Accretion Important E m w e Source Stream Accretion Flow Withdrawal 4 0 values indicate that no accretion flows or Node km Flow cms Temp CO Flows cms 51 54 e Mass Transfer Inflow 51 43 Locations should be input in 0 0 q nl withdrawals are occurring ol D T ae U J the downstream direction 3 0 0 0 Mass Transfer Inflow Locations Inflow Temperature Data C gt Inflow Heat 1 1 te He Locational Mass Source Inflow Inflow Inflow Inflow Information Transfer Node Stream Rate Temp Rate Temp optional Process optional km Time cms CC cms cc Copper Creek 103 46 393 6 14 99 12 00 AM 0 72 4 74 O 1430038 47407407 From Catched Twa Lk 2 169 43 09 61499 1 00 AM O72 4 519 0 1430038 4 5165155 E Lostine River 4 186 42 24 of 14 99 2 00 AM 0 72 4 3 0 O 1430038 4 5703704 Trib on AB amp LE 4 226 40 24 6 14 99 3 00 AM 0 72 4 370 O 1430038 4 5703704 Trib on LB z 260 38 54 814799 4 00 AM 0 72 4 3 0 O 1430038 4 5703704 Spring on AB 5 26a 38 14 8 14 99 5 00 AM 0 72 4 296 O 1430038 4 2962963 Page 110 Chapter IV Model Operation Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for
160. ient and Huber 1992 Kinematic Wave Equation aQ aQ a7Q bea Pcia E p a 1 a Ck a a 3 19 Wave Celerity cx Bedient and Huber 1992 o 22 sus ai Si PE 3 dA 3 n Diffusion Coefficient D Bedient and Huber 1992 D x 04 ax 3 21 The weighting factor 0 lt X 0 5 can be calculated or input by the user Bedient and Huber 1992 1 Q Q l W x 1_ Dx _1 2 W S _1 1 Ww So 3 22 2 Ck dx 2 Ck dX 2 Ck dX 15 The weighting factor X will be zero when there is no wedge storage in most cases this term is zero in reservoirs and greater than zero in flowing stream and river reaches For natural river flows X will usually be between 0 1 and 0 3 with an average value of 0 2 Page 79 Chapter IIl Dynamic Mass Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 The Muskingum coefficients are calculated as follows Bedient and Huber 1992 c at 2 K X c t 2 K x D D jn D 2 K 1 X dt gt C C C C C 0 3 23 The Muskingum method finite difference form of 3 19 then becomes Qik C Qi Cz Qi C3 Qi 3 24 t 1 FIGURE 3 5 Muskingum Cunge Finite Difference Scheme t 1 i 1 i i 1 Page 80 Chapter IIl Dynamic Mass Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Variables Measured Known dx Model
161. iid prred Palalive Air Tarip Sliir Vand spre TERNE hair negi Er imes Hamiin h W Temp ti ima Hiaiciiry uss Eee at Coe 18 a5 aS 19 rere En ae h Dat bahra im ETEN j J i Eat ois h et i u E lma ingie Eain tJ a Ty i tale Bboy cede fea a Ha ee Reese Continuous Data Node Heat Source Locations will control Hode where these data are used in the model Locational Continuous Information optional Hode optional Stream km d s E Lostine F 41 89 SWED monitoring site 16 84 E Confauous Continuous Confnuous Continuous Boundary Conditions Data Node 1 Data Node T Data Node 1 Data Node 1 Stream Temperature Cloudiness Wind Speed Relative Air Temp Stream Time Flow cms C 0 1 m s Humidity 7 C Temp C 8 14 99 12 00 4M a a H4 991008M 0673903061 8 0 Oo 8 amp 8 0 states P s PREE PENE ts T ET E E E ELS en P SE T Chapter IV Model Operation Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 4 3 4 MODEL SETUP MASS TRANSFER DATA Mass transfer data include site specific at discrete locations surface and subsurface inflows These flows do not including hyporheic exchange inflows accretion distributed inflows and withdrawals Double clicking on the number of inflow data sites allows the model to format the Flow
162. ill yield accurate reference points for sampling a IN x i mG 214 feets a Eno er FIGURE5 2 ieee Comparison of Stream Position 7 em e Mapped at 1 100 000 and 1 5 000 KES Sa ee TA e Scales Measurements in white s e ITO See ndicate Horizontal Positional feet 3 7 SE Errors in the 1 100 000 Scaled Stream Layer Rectified Page 141 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Digitized stream position is used to develop data nodes reference points for sampled derived data generated with the TTools extension Once a stream polyline has been digitized it is segmented at a user defined interval to produce a point data layer shapefile This point data theme is then used to sample other parameters and data generated is associated with these discrete points A common longitudinal sampling distance is 50 meters oe MSN i 4 an a Ty AE i k i g ad Mh s 4 i zA a Tm ee ia FIGURE 5 3 Digitized Stream Position Polyline and Segmented Stream Data Nodes Point Layer Segmented at 50 meter Interval Mapped at 1 5 000 Scale 5 3 2 STREAM ASPECT The stream aspect is defined as the angle that exists between the velocity gt vector U and true north 0 TTools calculates this angle as the angle between each of the stream data nodes see Figure 5 4
163. inite difference distance and time steps may be creating model instability If the problem persists when distance steps and time steps are reduced i e dx 100 m and dt 1 minute then the source of the instability is likely an input entry error Nonnumeric input values will cause model problems Null values in the input data set also may crash the model Unless noted in the worksheets all white cells should contain the appropriate model input except in the Land Cover Codes and Validation Data worksheets o Inaccurate or Sparse Meteorological Data When simulating over long distances in the Pacific Northwest you will likely traverse variable land cover and topographic conditions that will affect the local microclimates Further the adiabatic lapse rate will generally reduce atmospheric pressure affecting vapor pressures and the vapor pressure deficit cool the air temperature as a function of increasing elevation and affect wind speed variability This problem is only truly addressed with multiple atmospheric data measurement locations along the simulated stream network However such data will often be a limiting factor in model accuracy o Diurnal Water Temperature Sometimes simulated stream temperatures will under or over predict when compared to measured diurnal changes Recall that stream temperature change is inversely proportional to flow 18 View to sky is not a function of time day Page 133 Chapter IV Model Ope
164. ion is a closer to the convergence final approximation condition Further the substrate temperature is also assumed to equal the initial condition temperatures and will require more simulation time to reach a dynamic equilibrium heat transfer condition note this does not imply thermal equilibrium with the water column Page 69 Chapter Il Heat Transfer Page 70 Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 t 7 t 7 i 1 i 1 O Node used in time difference O Node used in second derivative space difference xX Node used in first derivative space difference FIGURE 2 6 MacCormick Finite Difference Scheme t 1 t 1 Boundary Condition Data Input i i 1 i i 1 ys t 0 Olw Initial Values Tw Twi 0 FIGURE 2 7 Boundary Conditions and Initial Values Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Chapter Dynamic Mass Transfer Description of Processes Analytical Methods and Finite Difference Approximation 2 a SS i F aA f Mass transfer is simulated as a function of the St Venant equations which combine continuity and momentum picture Trask River Oregon 3 1 OVERVIEW Mass transfer processes refer to the movement and mixing of water throughout a stream system The downstream transport of dissolved suspende
165. ion of the sun It can also be explained as the apparent solar time minus mean solar time The equation of time is calculated as a fairly complex expression below Equation of time minutes 4 O E 4 A B 2 E Ci died Eg A C D 2 A2 E S 8 F 12 TU 2 17 where 2 TU i TU i TU A tarf oos s as B sin 2 e Ors G Sinf ozs s 5 TU TU TU D Cos 2 6 E Sin 4 0 _ F Sin 2 6 _ sd a a i a _ The apparent solar time is a measure of time based on the diurnal motion of the true Sun The rate of diurnal motion undergoes seasonal variation because of the obliquity of the ecliptic and because of the eccentricity of the Earth s orbit Additional small variations result from irregularities in the rotation of the Earth on it axis Solar time ts is calculated as a function of the daylight savings time Astronomical unit AU is the radius of a circular orbit in which a body of negligible mass and free of perturbations would revolve around the Sun in 2r k days where k is the Gaussian gravitational constant This is slightly less than the semi major axis of the Earth s orbit Page 34 Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 tost equation of time E longitudinal position on earth longitude On time zone tone and of time measured in Julian centuries type Solar Ti
166. is will move the frame over so you can continue digitizing 15 To stop drawing the stream line double click HERE ARE SOME TIPS REGARDING THIS STREAM DIGITIZING PROCESS Save your work often To do this go to Theme Save Edits Save each stream that you digitize as a separate theme If the channel splits trace only one channel whichever appears to be the main one Remember to use that Snap tool in order to minimize cleaning up that you have to do later lf you are trying to digitize a stream in a heavily forested area which is likely to be the case in an upper watershed area you may also need DRGs for the area DRG stands for Digital Raster Graphic The DRG for a particular quad is simply the scanned version of the USGS topo map for that area The scale for DRGs is therefore the same as that for USGS topo maps or 1 24 000 Because we are interested in developing stream and vegetation layers that will be accurate to 1 5000 DRGs may be used as a point of reference when the aerial imagery for a particular area is difficult to read but they are not a substitute for developing stream or vegetation layers from aerial imagery You will not know if you need to obtain DRGs to create a stream layer until you have worked with the aerial imagery for awhile If you do decide you need them they can be obtained through the following website www reo gov This is the website for the Regional Ecosystem Office which is part of the Northwest
167. isplays longitudinally sampled channel width for the Williamson River Oregon Left Channel Edge Right Channel Edge FIGURE 5 5 Channel Width Sampling from Digitized Channel Edges at Each Stream Data Node Page 143 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Digitized Channel Edges and Stream Data Nodes Williamson River Oregon T 250 D 200 2 150 Sampled Channel Width D 100 Williamson River Oregon E 2 50 7 yD oO K O Q TM w Lr Ly Ly Ly uo iio Li 3 FA D amp ese Statistically Assess Sampled Channel Width Accuracy Williamson and n 48 R2 0 94 Sprague Rivers Oregon Se 16m 5 2 ft Dey 1 3 m 4 3 ft Significant at 0 05 sampled Estimate 0 10 20 30 40 SO BO FO BD Y 100 Ground Level BFW FIGURE 5 6 Digitized Channel Width Sampling Results and Validation Statistics Page 144 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 5 3 4 NEAR STREAM LAND COVER MAPPING FROM AERIAL IMAGERY The role of near stream land cover in maintaining a healthy stream condition and water quality is well documented and accepted in scientific literature Beschta et al 1987 Near stream land cover has several influences upon the stream and the surrounding environment
168. l geometry and Manning s equation A system of equations is developed for cross sectional area Aw wetted perimeter Pw hydraulic radius Rn and flow volume Q A U that become a function of known variables and one unknown variable wetted depth dw Convergence on the value of wetted depth the root for the system of equations is performed by the Newton Raphson root finding iterative method The use of Manning s equation relies on the assumption that flows are steady 2 0 and uniform o over the length of a stream segment i at any t X particular time t This methodology when combined with a finite difference approximation of the St Venant Equations allows for calculation of unsteady flows Ga between time steps t t and non uniform flows 0 for each X stream segment i Bedient and Huber 1992 Width FIGURE 3 3 Channel Cross Section Represented as a Trapezoid and Calculated Dimensions Depth Width Bottom 14 A stream segment is defined as the length of stream that spans one model distance step dx and is denoted in listed equations with the subscript f Page 73 Chapter IIl Dynamic Mass Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Manning s Equation Ta al U Rp3 Soe 3 1 Flow Volume 2 1 Q A U 2 Ay Ry3 So 3 2 Hydraulic Radius A R a 3 3 Cross Sectional Area
169. lated as the volume weighted average of each medium The thermal conductivity is a calculated as the product of density thermal diffusivity and specific heat capacity The conduction flux can be calculated as a function of the conductivity of the conduction layer and difference between the conduction layer temperature and water column temperature Recall that during periods of solar exposure i e daytime that the substrate will attenuate a portion of the radiant heat reaching the stream bed This heat changes the temperature of the conduction layer and is accounted in the heat budget A secondary heat transfer occurs between the substrate conduction layer and deeper alluvium The conduction layer temperature will change at different rates than the water column allowing for Page 54 Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 varying thermal gradients over time and space The conduction layer initial temperature condition is assumed to be equal with the stream node initial condition Conduction represents a change in heat and is accounted for in the conduction layer heat budget and temperature It should be noted that all solar heat is conserved In effect a portion of solar heat energy is routed through the substrate and either remains in the substrate or is returned to the stream system via conduction Further conduction can transfer heat f
170. lds 1 e z 1 dw dw dw i Uia U Pa oo wis dwi 0 dt 2 dx 2 dX Which is rearranged to represent the Finite Difference Form of the Continuity Equation dt 5 E dwi dw t Sood Ua URL UP wit awia 3 26 Substitution into 3 14 Conservation of Momentum Equation yields t 1 t 1 t 1 t 1 Ui Uia dwin dwi UU Uu g So S dt 2 dx 2 dX Which is rearranged to represent the Finite Difference Form of the Conservation of Momentum Equation 3 14 4 dt 4 itt Ui U SU Ut u dt 24 foni dwi dt a Go S 27 Page 82 Chapter Ill Dynamic Mass Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 t 1 t 1 For a trapezoidal channel where U Vier FU the friction slope becomes 2 Uir Ui we 2 U n U n U n Ans Fal ii dw Ws Fy an ee Wp 2 dw v 1 Z Substitution of 3 28 into 3 27 provides the final finite difference form of the Conservation of Momentum Equation 3 28 t 1 4 dt a yt 1 dt Ui U are ra 7 R Eal 3 ae ad 2 dx 2 0 0 S0 nme ese aiez ai 2 m t n 3 29 Wp 2 dw V1 Zz FIGURE 3 6 Explicit Finite Difference Scheme i 1 i i 7 COURANT STABILITY FRICTION STABILITY dx dx dt lt eee 3 30 Rp U c U 4g dw e T 3 31 Page 83 Chapter IIl Dynamic Mass Transfer Analytical Metho
171. le for assessment and input into the Heat Source methodology Page 146 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Example of Polygon Mapping of Near Stream Land Cover from Aerial Color Imagery Williamson River Oregon At this point only the line work is complete and no data is associated with the polygons Example of Classification of the Land Cover Polygons Associating a Land Cover Type to Each of the Polygons Williamson River Oregon At this point a land cover type numeric code is associated with each polygon Land Cover and g DE ft Sarnyaling O clot o green dots O TTools radial sampling pattern for near stream land cover sampling interval is user defined Radial land cover sampling occurs for every stream data node at four user defined intervals in the northwest west southwest south southeast east and north east directions North is not sampled since the sun does not shine from that direction in the northern hemisphere and shadows will hence not be cast in a southerly direction A database of land cover type in created for each stream data node cy 43 Page 147 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 USFS Data Collection Sites L
172. les to the water column and represents heat gain to the water column Condensation occurs when the water vapor deficit is directed form the overlaying air mass to the water column and predicted when the air temperature is below the dew point i e the air mass is saturated with water vapor Water molecules in the liquid phase require energy to overcome the molecular bonds that bind the liquid molecules The energy needed to change water from a liquid to gaseous phase is known as the atent heat of vaporization Page 58 Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Heat energy necessary for the evaporative process is furnished by the stream system and transferred to the surrounding air mass representing a net heat energy loss Sensible heat exchange is an upward rate of turbulent heat transfer and is limited by the density and heat capacity of air The evaporative heat flux across the air water interface is generally the most significant factor in dissipation of stream heat Parker and Krenkel 1969 Special consideration must be taken in addressing the simulation of evaporation rates since the evaporation flux is the energy process in which streams dissipate most heat energy and therefore contributes most to decreases in water column temperature Further the evaporation flux is utilized by the Bowen ratio to approximate the convective heat e
173. logy and morphology parameters and variation is a common challenge before us Identifying specific limitations increases analytical credibility and focuses our efforts on future monitoring and analytical advancements e Atany scale it is challenging to capture spatial variability in stream and landscape data Ground level measurements are particularly unsuited for detecting spatial variability e Simple instream measurements of flow above and below a study reach can be insufficient to detect subsurface interactions with the stream due to instrumentation limitations Without remote sensing such data may not describe high resolution instream flow conditions making validation of derived mass balances difficult While analytical techniques exist for describing subsurface stream interactions they may be beyond the scope of an effort with regard to data availability technical rigor and resource allocations e Water quality issues are complex and interrelated The state of the science is still evolving in the context of landscape scaled water quality analysis The degree to which one parameter affects another may not be fully understood Analytical methods may capture primary effects but miss secondary more subtle effects An example is the relationship between channel form function and flood plain land cover distributions While both can be quantified independenily the extent that each affects the other may be variable and or site specific and
174. luvium The alluvial aquifer refers to the water that occupies the interstitial soaces in the alluvium This water moves directionally based on the elevation of the stream water column relative to the shallow groundwater elevation If the shallow ground water elevation is lower than the surface water column elevation the potential energy gradient will be directed away from the stream In this case water will likely be lost from the stream to the alluvial aquifer If this water stays in the alluvial aquifer and is not lost to deeper subsurface storage less prone to be connected to down gradient surface waters it will reemerge back to the surface water column when the potential energy gradient is directed from the alluvial aquifer to the stream The rate of hyporheic water movement depends on the hydraulic head potential energy and physical properties of the alluvium Consider that water is incompressible If we assume that water lost to deeper ground water sources is negligible then a discrete volume transferred to the alluvial aquifer from surface waters must result in an equal volume transferred back to surface waters from the alluvial aquifer Page 94 Chapter Ill Dynamic Mass Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Thermal Infrared Over Multi Spectral Image Thermal Infrared Calor Map imc girs 15 C p S N orc 3 al i j
175. ly close out of ArcView and re open the project before beginning this step of TTools Doing so will clear ArcView and Spatial Analyst memory and TTools will then be able to accurately predict and prevent a potentially disastrous crash Page 179 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 PREREQUISITES e You must have your TTools point theme in the view e You must have a riparian vegetation grid theme in the view e You must have your DEM in the view Helpful Hint Before proceeding with TTools sampling make sure that your DEM vegetation grid and T Tools point coverage are located on your local hard drive If your DEM or vegetation grid resides on a network drive TTools sampling will take about three times longer STEPS 1 Select the Sample Riparian Land Cover option in the TTools menu 2 Select your TTools point theme 3 Select your 1 5000 digitized riparian vegetation grid theme 4 Select your DEM 5 Select your DEM elevation units 6 Type in your sampling distance interval in meters This is the distance between sampling steps 7 Spatial Analyst developed by Esri has a bug which limits the number of grid samples that it may perform Beyond which ArcView fatally crashes and reports a Segmentation Violation error TTools will prevent this disaster from happening Depending on the size o
176. maximum daily water temperature Beschta and Weatherred 1984 This is largely because a portion of incoming solar heat is routed through the sediments to the water column instead of directly attenuating in the water column For the purposes of developing the conduction heat flux analytical methodology the morphologic terminology requires definition Substrate is comprised of various types and sizes of alluvium that occupies the stream bed Alluvium consists of depositional materials and substrate that underlies the stream channel Alluvium material is sorted to some degree by tractive forces and shear stress associated with surface high flow conditions The distribution of alluvium can vary significantly within the channel and across the floodplain The depth of alluvium will vary by site and is not predictably quantified without accurate ground level geologic and hydrologic information The supply of sediments and the flow patterns during peak events affect the distribution and type of sediment found in the alluvium Porosity refers to the interstitial TABLE 2 2 Bed Particle Size Bedient amp Huber 1992 Rosgen 1996 spaces void space in the alluvium Size Class dso and is assumed to be filled with fine Silt lt 0 062 mm sediments and water Estimates of Sand 0 062 2 0 mm porosity are made as a function of substrate size with an Gravel 2 0 63 5 mm acknowledgement that such an Cobble 63 5 254 mm assumption is a simplification
177. me minutes ts 60 h m4 E E 4 Dong 00 ig 2 18 Hour angle is the angular distance on the Earth s sohere measured westward along the equator from the meridian to the hour circle The hour angle 644 is calculated solely as a function of solar time ts Hour Angle 0 84 lt 360 Ou 180 2 19 Variables Measured Known h Hour based on daylight savings time hr m Minute based on daylight savings time min s Second based on daylight savings time sec trone Time Zone see Table 2 1 Oiong Longitude degrees Calculated Solar Declination degrees Ec Eccentricity of Earth s Orbit unitless E Equation of Time minutes O Apparent Longitude of the Sun degrees 9x55 Geometric Mean of Anomaly of the Sun degrees Ocs Equation of the Center of the Sun degrees Qua Hour Angle degrees 9 5 Geometric Mean of the Longitude of the Sun degrees 908 Obliquity of the Elliptic degrees Ota Solar True Anomaly degrees P Solar Radius Vector AU ts Solar Time minutes Page 35 Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 2 2 3 SOLAR POSITION RELATIVE TO STREAM POSITION The uncorrected solar zenith refers to the point at which the sun is directly overhead of the Earth s sphere The geocentric solar zenith is defined by the line from the center of the Earth through the obser
178. me simple examples of riparian feature codes and descriptions They may vary in type and complexity depending upon the sub basin or stream that is being analyzed Page 172 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Height Density Code Riparian Feature Description m Water 0 0 0 River Bottom Floodplain 0 0 0 0 0 0 3011 302 302 30 30 30 30 30 Pastures Cultivated Field Lawn Young Orchard Mature Orchard Barren Rock Barren Embankment 0 0 0 0 Barren Campground Park 0 0 0 0 0 0 7 7 0 0 Barren Gravel Pit 0 Barren Clearcut 0 0 0 0 Qo Q 309 Clearcut below 50 dense 2 regeneration 321 Lumber Yard 0 0 40 Barren Road 0 0 0 0 Barren Forest Road Barren Railroad 0 0 0 0 Barren Ag Road 500 Large Mixed Conifer Hardwood 7 gt 75 Canopy 2 501 Small Mixed Conifer Hardwood 1 i 1 0 0 O 40 P gt GO PO O gt 75 Canopy 4 550 Large Mixed Conifer Hardwood 2 gt 25 Canopy 0 6 4 2 4 551 Small Mixed Conifer Hardwood 2 2 9 6 6 0 1 1 gt 25 Canopy Large Hardwood 2 Small Hardwood Large Hardwood Small Hardwood Large Conifer Small Conifer Large Conifer 2 Small Conifer 2 Shrubs
179. mic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 4 4 3 EXECUTABLES HEAT SOURCE Heat Source is the combination heat and mass transfer models Page 126 Info General Model Input Model Setup Executables Diagrams Shade a lator Application Simulate heat transfer Heat Source dynamic flow routing Purpose wetted channel E ah a noes simulate stream temperature via dynamic dimensions and Heat Source pie eae Sno hydraulics including simulation occurs over the defined stream network during the hvyoorheic flows and period specified Output is provided at the defined distance step i and can be found on all of the output and chart worksheets WAEI COMMI temperature Emergent vegetation can be incorporated into the solar routing methodology This is commonly used when simulating wetlands Inputs All of the heat transfer input sheets should be completed Fa Oregon 2 Department of a Environmental Quality Hide Main Menu e Outputs All of the Before you run Heat Source enter h Ib all data found on all input sheets output sneets will be completed Account For Emergent Vegetation Aooraonate model use and aooication are the sole responsibility of fhe user Pie OUr S i Bak to 70 a r _ pr x F ail p7 Chapter IV Model Operation Analytical Methods for Dynamic Open Channel Heat and Mass Transfe
180. ming that heat transfer and turbulent mixing are responsible for the transport of momentum heat and water vapor in the atmospheric boundary layer directly above the stream surface McCutcheon 1989 Evaporation is an extremely important area of hydrologic study For example in the United States 70 of the received precipitation is returned to the atmosphere via evaporation and transpiration Dingman 2002 Accurate water balance and heat balance methods must devote considerable attention to robust analytical treatment of evaporative water loss It follows that the evaporative process has been the topic of vigorous research Several Page 59 Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 methods namely the mass transfer method energy budget method and the combination method are available in the literature and are described below MASS TRANSFER METHOD A primary focus on the turbulent transfer of water vapor from a waterbody to the atmospheric air mass allows a simple expression of evaporation as an approximation of the vapor gradient e e and the movement of the air W directly above the water surface width of exposure Numerous expressions closely follow Dalton type equations similar to Equation 2 96 Special attention should be paid to the measurement height above the free water surface for the input variables wind speed ai
181. mized since instream flows will be very small relative to the inflows and the inflow temperatures should dominate 3 8 TENDENCY TO STRATIFY Martin and McCutcheon 1999 present the densiometric Froude number as a measure of the tendency of a water body to stratify Norton et al 1968 first developed the densiometric Froude number and used it for prediction of Stratification potential of reservoirs Page 99 Chapter Ill Dynamic Mass Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Densiometric Froude Number r 1 Qa i a 3 45 g e dw V g e dw A Variables Measured Known dx Model Distance Step m g Acceleration of Gravity 9 8 e Density Gradient 10 Calculated A Cross Sectional Wetted Area m dw Average Water Column Depth m F Densiometric Froude Number unitless Fy gt 1 25 Low Tendency to Stratify 0 75 gt Fa lt 1 25 Moderate Tendency to Stratify Fy lt 0 75 High Tendency to Stratify Q Flow Rate m V Water Column Volume m Page 100 Chapter IIl Dynamic Mass Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Chapter Model Operation VV Input Data Procedures and Modules 4 1 OVERVIEW Important Analytical methods are presented in preceding Chapters l Ill and can be found in the Visual Basic programming in the mod
182. mulative impacts of mass and heat transfer The list of questions directed at a stream temperature analytical effort can often be quite long and is always much longer than the list of preceding questions Regardless of whether the study area is large and complex or simply a stream segment a primary question posed in this section is what is a comprehensive assessment The answer to this question seems to have changed recently as data collection and analytical techniques have evolved over past several years A comprehensive assessment utilizes integrated remotely Page 4 Chapter Introduction Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 sensed and ground level continuous temperature data weather data channel morphology hydraulics and near stream land cover data Sampled GIS data should be incorporated into the analysis for many of these parameters When possible thermal infrared remote sensing should be used to quantify stream mixing thermal gradients and mass transfer processes that cannot be measured at the ground level Other forms of spatial data allow quantification of topography and land form Model inputs can be dramatically improved simply by drawing from morphologic and land cover assessments methods i e Kovalchik 1987 Hall 1998 Rosgen 1996 Amidst these advances some factors have remained constant You will not have all the data that you want
183. n creating a tradeoff between model resolution and computational efficiency 4 3 GENERAL SETUP PROCEDURE A general setup stepwise procedure can be summarized as follows Step 1 Complete data fields text boxes found in the General Inputs tab from the Main Menu Step 2 Setup the spatial data worksheets from the Data Sheets tab Step 3 Setup the temporal data worksheet from the Continuous Data tab Step 4 Setup the flow data worksheet from the Mass Transfer Data tab Step 5 Assign physical attributes to land cover classifications Enter codes and associated physical attribute information into the Land Cover Codes worksheet Run Vegematic to assign height density and overhang information to sampled land cover classifications Stability criteria are a function of the selected finite approximation methods Heat transfer methods are highly stable Mass transfer stability criteria are listed in Table 3 1 Page 102 Chapter IV Model Operation Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Step 6 Enter morphology input data Either enter or assign W D based on Rosgen Level information under the Associate W D tab Calculate the bankfull morphology under the Bankfull Morph tab Step 7 Select evaporation rate model and a and b constants under the Evaporation tab Step 8 Select dynami
184. n instantaneous path length estimated as the optical air mass thickness M4 Direct Beam Solar Radiation above Topographic Features Estimate Wunderlich 1972 Martin and McCutcheon 1999 Dopp SRG Ta 1 0 65 C 2 29 Page 38 Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Atmospheric Transmissivity Ibqal 1983 T 0 0685 Cos 2 2 UD 10 0 8 365 2 30 Optical Air Mass Thickness lbgal 1983 35 g 0 0001 184 Zs Ma 1224 Sin Osa 3 2 31 TU e Direct Beam Solar Radiation above Topographic Features Chen 1994 Psrei Pgpp N1 DF 2 32 Diffuse Solar Radiation above Topographic Features Chen 1994 Psroi Psapp DF 2 33 Clearness Index Chen 1994 C P spp D sre 2 34 Diffuse Fraction Chen 1994 Dp 0 988 1 071 C 5 14 C 2 98 6 Variables JD 40 2 35 365 l Si 2x 0 009 0 078 C Measured Known Ci Dspc JD tpst Zs Calculated C Dg gt P spe P spg P srp1 P sra Ma Osa i Ta Page 39 Cloudiness 0 to 1 Solar Constant a Julian Day 1 to 365 Daylight Savings Time day fraction Stream Elevation m Clearness Index Diffuse Fraction of Solar Radiation Direct Beam Solar Radiation Estimate above Topography ea Direct Beam Solar Radiation above Topography
185. nce it eliminates the problems associated with the mass transfer and energy budget methods Combination Method Penman Evaporation Rate basic form E Energy Input Mass Transfer 2 104 Combination Method Penman Evaporation Rate Dingman 2002 E solar FOr A ee y Pho Le A y A y salar t oranan A E y ee 2 105 A Y Slope of the Saturation Vapor v Air Temperature Curve Dunne and Leopold 1978 1727 1 17 27 Ta 1 A as 6 1275 2373 TA _ 4975 eh 2873HTa t 2 106 s s a Page 61 Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Psychrometric Constant Cuenca 1989 y 1003 5 AE 2 107 0 62198 L Aerodynamic Evaporation Dingman 2002 Ea f W le e 2 108 2 4 2 WIND FUNCTIONS Both the mass transfer and the combination Penman method utilize a wind function f W to estimate adiabatic portion of evaporation In essence the wind function has the following form Wind Function Shanahan et al 1984 f W a b W where a and b are coefficients see Table 2 3 W Wind velocity measured at 2 meters above water surface 2 109 Table 2 3 Wind Function Coefficients a b Source Location mb ms mb Meyer 1928 4 18 10 0 95 10 Marciano and Harbeck 1952 Lake Hefner 0 1 02 10 Harbeck et al 1959 Colorado City 0 1 51 10 Morton
186. nd on local drives Be careful before deleting data and be sure that you always have a previous version of your work saved Excel has known bugs that will crash the model unexpectedly and you should anticipate such problems The authors also recommend that you refrain from working directly from networks or servers due to a known Excel problem with completing large saves over networks Several message boxes will ask the user to confirm that they want to delete input data Configuring the longitudinal data inflow data sites and continuous data sites involves changing location and temporal data in the model The user is asked whether they want to delete the current inputs associated with existing longitudinal or temporal data since these data are about to be changed If the user can keep track of existing data associations it may be easier to choose not to delete existing data and simply move it appropriately after the location or temporal setup configuration Page 134 Chapter IV Model Operation Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Code Execution Has Been Interrupted This is a very common Microsoft message box that notifies the user when VBA code has been stopped You can trigger a code interruption by pressing the control and break keys at the same time ctrl break This message will also appear when an irresolvable error occurs such as division by zero ille
187. near field search distance is 750 meters 2460 feet Page 150 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 topographic shade angle for all three directions is stored in memory for each stream node The far field search for the maximum topographic shade angle typically targets large features hills mountains etc and spans greater distances from the stream These factors allow fewer restrictions for sampling resolution and allow greater sampling interval distances Computationally this is very important because grid data sampling can be long and expose ArcView bugs that may interfere with application functions The user is allowed to enter the far field sampling interval and the distance to sample The higher of the two maximum topographic shade angles near field and far field is entered in the stream node database FIGURE 5 11 Near and Far Field Topographic Shade Angle Calculations from DEM Data Near field Far Field Each of first 25 DEM User determines sample cells is sampled distance and interval TTools records the max topographic shade angle Topographic Shade Calculation o tan 5 2 Ly Variables Measured Known dx Distance Step m i Stream Data Node L Distance from Stream Data Node i to topographic feature z Elevation s Z Elevation of Topographic Feature s Cal
188. nergy flux and thus the accuracy of the convection flux is dependent on accurate estimation of the evaporation energy flux The vapor pressure gradient between the water surface e and the air ea directly above the stream drives evaporation i e the vaporization of water molecules when the gradient is positive e lt e Only when the air is saturated does evaporation cease to occur ea es This condition is known as the dew point temperature The overlying air mass may become supersaturated with resulting condensation when the vapor pressure gradient is negative ey 2G The evaporative flux can be calculated as a summation of the sensible heat carried with evaporated water vapor and the product of the latent heat of evaporation LHV density of water pw and the rate of evaporation E The energy needed for water to change from a liquid to a gas the latent heat of vaporization LHV is a function of water temperature McCutcheon 1989 Brown and Barnwell 1987 found that for practical modeling applications the sensible heat term convection IS Negligible however convection heat transfer is included in this methodology and is described in the following section Evaporation Flux evaporation PH 0 Hbg E 2 94 Latent Heat of Vaporization La 1000 2501 4 1 83 Ty 2 95 Evaporation Rate E is defined in the following section 2 4 1 EVAPORATION RATE The rate of evaporation is derived by assu
189. ngs and Accretion Flows 93 3 4 5 Hyporheic Flows 94 3 4 6 Evaporation Losses 97 3 5 Flow Volume Continuity 98 3 6 Controlled Flows and Depths 99 3 7 Dewatered Channels 99 3 8 Tendency to Stratify 99 CHAPTER IV MODEL OPERATION 4 1 Overview 101 4 2 Finite Difference Steps 102 4 3 General Setup Procedure 102 4 3 1 General Inputs 103 4 3 2 Model Setup Data Sheets 104 4 3 3 Model Setup Continuous Data 105 4 3 4 Model Setup Mass Transfer Data 108 4 3 5 Model Setup TTools Data 111 4 3 6 Model Setup Land Cover Codes and Attribute Associations 111 4 3 7 Model Setup Morphology Data 113 4 3 8 Model Setup Evaporation Rate Methods 118 4 3 9 Model Setup Stream Bed Conduction 119 4 3 10 Model Setup Physically Based Flow Routing Methods 120 4 3 11 Model Setup Clear All Data Sheets 121 4 3 12 Model Setup Validation Data 122 4 4 Executables 123 4 4 1 Executables Shade a lator 124 4 4 2 Executables Flow Router 125 4 4 3 Executables Heat Source 126 4 5 Model Outputs 127 4 5 1 Chart Diel Temperature 127 4 5 2 Chart TIR Temperature 128 4 5 3 Chart Longitudinal Temperature 129 4 5 4 Chart Solar Flux 129 4 5 5 Chart Heat Flux 130 4 5 6 Chart Effective Shade 131 4 5 7 Other Output Data Worksheets 131 4 6 Common Sources of Problems 133 4 7 Dialogue Windows Purpose and Meaning 134 4 7 1 Progress Window 134 4 7 2 Message Boxes 134 4 8 Other Utility Applications 137 4 8 1
190. nput parameters even those Page 3 Chapter Introduction Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 considered by some to be less important and or too difficult to quantify Simply stated model robustness is also derived from high input data resolution in addition to the analytical methodology scope and input data types The authors contend that coarse application of the methodology will cause output errors the model will perform poorly because the impacts of human landscape and hydrologic influences often occur at a high spatial resolution Observed or simulated stream temperatures result from a multitude of parameters and processes Even small changes or omissions in these parameters or processes both thermal and hydrologic may cause significant temperature changes By definition such changes are cumulative effects The methodology is intended to be applied over large scales i e network scale with the intent of capturing cumulative effects These forms of robustness manifest themselves with results that are typically accurate data driven and inherently unbiased by underlying simplifications or assumptions because they are minimized to the best practical extent A New Way to Model Hydrology and Water Quality For these reasons Heat Source represents part of a growing shift in stream temperature analytical approach This shift is facilitated by the a
191. nto your project Name the point coverage that you are creating This will be the database file that TTools uses from here on out Do not use spaces in your file name or in the path to your file You will be asked if you want to Reverse Line Segments If you digitized your stream from the mouth up choose Yes Otherwise choose No If you are unsure just guess and you can check the results shortly You will be asked to input the spacing distance This determines the longitudinal distance between the nodes that will be placed on your stream polyline The units must be meters The Length column of your TTools point coverage now contains the cumulative longitudinal distance in meters The Aspect column contains the downstream segment direction units are degrees from north Important You MUST now double check the TTools point coverage that you created to be sure you did not select the wrong option when you were asked to Reverse Line Segments The following steps will guide you 1 Select your TTools point theme in your View 2 Select the uppermost point visible in your view the point nearest the headwaters 3 Open the Table to your TTools point theme Page 176 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 4 If the first record Id 0 is not highlighted then you made the wrong choi
192. ober then a correction for daylight savings time is made Page 30 Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 where A INT B 2 A INTIo 100 4 Julian Century typ tar 2451545 t aa 2 5 JDC 36525 2 5 Variables Measured Known D Day of Month 1 to 31 M Month 1 to 12 t Time day fraction trone Time Zone see Table 2 1 Y Year If month is less than 2 then Y Year 1 Calculated typ Julian days since epoch 1900 January 0 5 ET toc Julian centuries since epoch 1900 January 0 5 ET tost Daylight Savings Time day fraction temr Greenwich Mean Time day fraction 2 2 2 SOLAR POSITION RELATIVE TO EARTH All expressions presented in this section are taken from Meeus 1988 and 1991 Definition of terminology taken largely from The Astronomical Almanac 1998 The mean plane of the Earth s orbit around the Sun is called the elliptic Obliquity refers to the angle between the equatorial and orbital planes of the Earth which is equivalently between the rotational and orbital poles Specifically for the Earth the obliquity of the ecliptic is the angle between the planes of the equator and the ecliptic The obliquity of the elliptic is a function of the mean obliquity 65 and time measured in Julian centuries typ Mean Obliquity of the Elliptic degrees 26 a Q 23 _ OB 60 2 6
193. of ground level riparian information so that you can comfortably assign species compositions and heights to the vegetation map that you are creating While collecting the data species height density be sure to record the precise location so that you can match that data to the aerial imagery The steps for creating the vegetation polygons from your buffer are described below Make sure that your aerial imagery and buffer polygon theme are in the view Zoom to one end of the buffer theme Open the table to your vegetation buffer theme Go to Table Start Editing Go to Edit Add Field Name the field something like Vegcode as a number field with zero decimal places Go to Table Stop Editing and save the changes Return to your view Go to Theme Start Editing 10 Select the polygon splicing tool Page 171 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 11 Working from the outside of your buffer inward begin outlining the various riparian features IMPORTANT NOTE Only create one polygon at a time i e do not splice more than one polygon or the records within the theme s table will be linked and adding the polygon attributes will not be easy 12 Now you have a choice You can draw all of the polygons in your riparian vegetation map then add the codes Or you can add the codes to th
194. ofiles should be considered estimates of a steady state flow condition Water withdrawals are not directly quantified Instead water right data is simply the upper limit of volume allowed to be withdrawn An assumption is made that these water rights are being used if water availability permits This assumption can lead to an over estimate of water withdrawals Water withdrawals are assumed to occur only at mapped points of diversion sites or those visible in TIR data There may be additional diversions occurring throughout the stream network small pumps piped flows etc This assumption can lead to an underestimate of water withdrawals and an under estimate of potential flow rates Return flows may deliver water that is diverted from another watershed In some cases irrigation canals transport diverted water to application areas in another drainage This is especially common in low gradient meadows cultivated fields and drained wetlands used for agriculture production When return flows are removed in the potential flow condition this assumption can lead to an under estimate of potential tributary flow rates 3 4 3 SURFACE INFLOWS SPRINGS TRIBUTARIES AND RETURN FLOWS Surface inflows tributaries springs and return flows are associated in the model with longitudinal stream distances and thus with model reaches The total number of model reaches is a function of the distance step dx which is user defined and the simulation longitu
195. ograph with the geometric qualities of a map The standard DOQ is black and white with a one meter pixel resolution color DOQs are also available for some locations Standard color aerial photographs can be digitally scanned georeferenced and rectified The product is similar to a DOQ but is multispectral and usually has less than one meter resolution In the very near future high resolution one meter or two meter pixel satellite imagery should become available Certain satellites can record full spectrum imagery for large geographic areas This imagery is most often georeferenced and can be collected at almost any moment Hence the satellite imagery is seamless and can be collected and available in very short time spans DOQs and rectified aerial photographs are used to map streams delineate riparian land cover and to identify previously unmapped features such as diversions small dams etc 5 3 1 DIGITIZED STREAM POSITION FROM AERIAL IMAGERY Stream polyline accuracy is a function of the mapping scale For example the figure below demonstrates that a stream polyline at 1 100 000 mapping scale red line simplifies sinuosity and has local horizontal inaccuracies of over 200 feet Sampling with a 1 100 000 stream polyline will result in inaccurate sampling reference points and simplified stream sinuosity As can be seen in the figure below a stream polyline digitized at 1 5 000 mapping scale will properly identify stream position and w
196. olar Radiation Penetrating Stream Surface a Diffuse Solar Radiation Penetrating Stream Surface aa 2 Direct Beam Solar Radiation Attenuated in Water Column 2 Diffuse Solar Radiation Attenuated in Water Column a Solar Radiation Attenuated in Water Column es Direct Beam Solar Radiation Attenuated in Stream Bed Symbols Analytical Methods for Dynamic Open Channel Heat and Mass Transfer SYMBOLS Page 185 sprp7 Dsp7 D solar PD total Methodology for the Heat Source Model Version 7 0 Diffuse Solar Radiation Attenuated in Stream Bed ee Solar Radiation Attenuated in Stream Bed a Solar Radiation Attenuated in Water Column a Total Heat Flux aa Densiometric Froude Number unitless Psychrometric Constant ae Wind Velocity Coefficient k 0 4 Travel time Parameter s Volumetric Weighted Thermal Conductivity m s C Water Thermal Conductivity 0 600 m s C Sediment Thermal Conductivity 15 977 m s C Dominant Substrate Hydraulic Conductivity m s Composite Substrate Hydraulic Conductivity Hour based on daylight savings time hr Hydraulic Head for Darcy Calculation m Hydraulic Head Across Seepage Face m Land Cover Height for each Zone m Porosity of the Stream Bed unitless Julian Day 1 to 365 Latent Heat of Vaporization Cr Air Mass Thickness Minute based on daylight savings time min Manning s Roughness Co
197. olume 1 Heat transfer relates to processes that change heat in a defined water volume There are several thermodynamic pathways that can introduce or remove heat from a stream For any given stream reach heat exchange is closely related to the season time of day and the surrounding environment and the stream characteristics Heat transfer processes can be dynamic and Chapter Introduction Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 change over relatively small distances and time periods Several heat transfer processes can be affected by human activities 2 Mass transfer relates to transport of flow volume downstream instream mixing and the introduction or removal of water from a stream For instance flow from a tributary will cause a temperature change if the temperature is different from the receiving water Mass transfer commonly occurs in stream systems as a result of advection dispersion groundwater exchange hyporheic flows surface water exchange and other human related activities that alter stream flow volume 1 2 1 COMMON NONPOINT SOURCES OF STREAM TEMPERATURE CHANGE A dominant purpose for analytical modeling is to quantify human related stream change Brown 1969 identified temperature change as a function of heat and stream volume 1 1 Using this simple relationship it becomes apparent that stream temperature change is a function of the heat
198. on 2 2 1 Solar Time Relative to Earth 2 2 2 Solar Position Relative to Earth 2 2 3 Solar Position Relative to Stream Position 2 2 4 Solar Radiation Heat above Topographic Features 2 2 5 Solar Radiation Heat below Topographic Features 2 2 6 Solar Radiation Heat below Land Cover 2 2 6 Solar Radiation Heat above Stream Surface 2 2 Solar Radiation Heat Penetrating the Stream Surface 2 2 8 Solar Radiation Heat Received by Water Column and Substrate 2 2 Longwave Thermal Radiation 2 3 Substrate Conduction Flux 2 4 Evaporation Flux 2 4 1 Evaporation Rate 2 4 2 Wind Functions 2 5 Convection Flux 2 6 Stream Temperature Simulation Method 2 6 1 Non Uniform Heat Energy Transfer Methodology 2 6 2 Finite Difference Approximation CHAPTER Ill DYNAMIC MASS TRANSFER 3 1 Overview 3 2 Channel Geometry amp Manning s Relationships 3 3 Dynamic Hydraulic Flow Routing 3 3 2 Muskingum Cunge Approximation 3 3 2 Explicit Finite Difference Method 3 3 3 Comparison of Methods 3 4 Quantifying External Mass Transfers Page Table of Contents N ON WO 21 23 24 71 73 76 78 81 84 87 Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 3 4 1 Temperature Change Resulting from Mixing 87 3 4 2 Thermal Infrared Radiometry Derived Mass Balance Approach 88 3 4 3 Surface Inflows Springs Tributaries and Return Flows 92 3 4 4 Subsurface Inflows Seeps Spri
199. orksheet Bankfull Morphology Rosgen Level Estimated Maximum Average Cross Stream Type Bankfull Bottom Bankfull Bankfull Sectional Channel Gradient Mannings n optional W D Ratio Width im Width m Depth mj Depth m Area m Angle z 18 0 015 6 00 6 000 O 570 1 570 0 750 4 500 1 98 44 0 015 3 00 5 000 0 510 1 130 0 620 3 120 1 98 3 6 0 015 5 00 5400 0 520 1 160 0 640 3 250 1 98 2 4 0 015 6 00 5 000 0 510 1 1350 0 620 3 120 1 98 Known Estimated Values of Bankfull Morphology Calculated Values of Bankfull Morphology Page 115 Chapter IV Model Operation Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 MUSKINGUM X FACTOR Users should reference Section 3 3 2 Muskingum Cunge Approximation used for dynamic flow routing for an overview of the Muskingum Cunge Method and the importance of the X factor parameter In summary the X factor ranges between 0 and 0 5 where a O value represents no wedge storage in reservoirs for example and 0 5 represents full wedge storage in the finite element method The average X factor in a flowing river reach is often approximately 0 3 If you plan to use the Muskingum Cunge dynamic flow routing method and we recommend Cross that for distributed stream network Sectional Channel Y Factor modeling that you use this method then Area im Angle z 0 00 5 you will either need to enter X factor values 4500 198 a2 that can
200. otal Heat Flux 4 Tw Water Temperature C kg a t Shear Stress U Average Flow Velocity S U Shear Velocity 2 Vw Water Reach Volume m Ww Wetted Width m Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 2 6 2 FINITE DIFFERENCE APPROXIMATION The methods employed to approximate the one dimensional heat energy transfer equation 2 118 is essentially the summation of thermodynamic heat energy exchange between the stream system and the surrounding environment and physical processes that redistribute heat energy within the stream system Boyd 1996 It is important to note that all heat energy introduced into the stream is conserved hydraulically redistributed and partially lost to the surrounding environment via heat transfer processes with the net result reflected in stream temperature magnitude Heat energy is transient within the stream system due to longitudinal advective and dispersive transfer of heat energy The net heat energy flux is calculated at every distance step and time step based on physical and empirical formulations developed for each heat component Any effort to accurately simulate stream temperatures must develop a finite difference approximation to the three modes of heat energy transport and change advection dispersion and heat transfer MacCormick 1969 demonstrates
201. perature Journal of Soil and Water Conservation 25 11 13 Brown G W 1969 Predicting temperatures of small streams Water Resour Res 5 1 68 75 Brown L and Barnwell T O Jr 1987 The Enhanced Stream Water Quality Models QUAL2E and QUAL2E UNCAS Documentation and USER Manual Report EPA 600 3 87 007 U S Environmental Protection Agency Athens GA Chapra S C 1997 Surface Water Quality Modeling Boston WCB McGraw Hill Chen Y 1994 Hydrologic and water quality modeling for aquatic ecosystem protection and restoration in forest watersheds a case study of stream temperature in the Upper Grande Ronde River Oregon PhD Dissertation University of Georgia Athens Georgia Cuenca R H 1989 Irrigation System Design An Engineering Approach Englewood Cliffs New Jersey Prentice Hall Inc Cunge K A 1969 On the subject of a flood propagation method Muskingum Method J Hyd Res vol 7 no 2 pp 205 230 Dingman S L 2002 Physical Hydrology 2 Ed New Jersey Prentice Hall Domenico P A and F W Scwartz 1990 Physical and Chemical Hydrogeology New York John Wiley and Sons Inc Dunne T and L B Leopold 1978 Water in Environmental Planning San Francisco California W H Freeman and Company Faux R N P Maus C Torgersen and M Boyd 2001 Airborne Thermal Infrared TIR Remote Sensing Application to USDA USFS Stream Temperature Monitoring Programs New Approaches for monitoring thermal var
202. pplication of model inputs derived from rich spatial data sources and analytically robust methods designed to analyze stream temperature dynamics at any level of complexity Rejection of model simplification and instead embracing the rigors of data and analytical complexity is the basis for the model Generalizations only apply to basic thermodynamic heat transfer physics and physically based processes mass transfer physics Generalizations of thermodynamic behavior cannot be made at all until that is a comprehensive data rich analysis has been conducted at a network scale An acknowledgement of thermal uniqueness requires investigators of water temperature dynamics to challenge generalizations in the literature and perform analysis without preconceived notions of parameter and process sensitivity and ultimately model outputs A COMPREHENSIVE ANALYTICAL APPROACH As a rule a comprehensive analysis should be data rich draw from deterministic methods operated at high resolution and provided statistically validated results So you want to complete a comprehensive stream temperature assessment Or perhaps you need to calculate the thermal effect of solar radiation exposure to a water body What is the thermal effect of a point source Each question raises others What are the flow dynamics inherent to a stream What heat transfer processes dominate and which are of lesser importance Which parameters are within human control What are the cu
203. r Methodology for the Heat Source Model Version 7 0 4 5 MODEL OUTPUTS 4 5 1 CHART DIEL TEMPERATURE Measured hourly stream temperatures can be plotted against the simulated values for each Continuous Monitoring Node When a model run is completed the Continuous Monitoring Node list box is updated however when the model is Opened and not run it will be necessary to press the Update List Box button Validation statistics are provided Important Use this worksheet to validate the model output against measured temporal data Chart Diel Temp Worksheet Page 127 Chapter IV Model Operation Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 4 5 2 CHART TIR TEMPERATURE Measured TIR stream temperature data can be plotted against the simulated values that are paired with the closest location and time to the TIR measurement Pairings are made during the simulation when and where they occur Validation Statistics are provided Important Use this worksheet to validate the model output against measured spatial data The example provided below would be considered a poor result Chart TIR Worksheet Page 128 Chapter IV Model Operation Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 4 5 3 CHART LONGITUDINAL TEMPERATURE The spatial distrib
204. r codes must be integers non zero values and physical attribute data must be numeric There cannot be skipped rows i e rows without information in between rows with information because the model routines see a blank row as the end of the data sequence These land cover physical attribute data will be associated with the classification data in the next step Due to the radial sampling pattern utilized where directional sampling occurs around each data node the data are well suited for directional shade simulation but are not easily summarized for graphical presentation Part of Vegematic accounts for the stream aspect and land cover orientation location and creates a left right bank summary of the land cover height and density While these data are not used in the simulations they should be used to quantify the spatial distributions of land cover physical attributes See columns DX gt EN on the TTools Data worksheet for these data Page 111 Chapter IV Model Operation Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Vegematic is a simple routine that associates organizes and summarizes the land cover physical attribute information Output data from Vegematic will be located in the TTools Data worksheet in columns BS gt FE Land cover physical attribute data used in solar routing and shade simulations can be found in columns BS gt
205. r heat flux that reaches the stream surface with shading and obstructions that attenuate and scatter shortwave radiation i e with land cover topography stream banks etc Cloudiness is accounted for in the Directly Above Stream solar heat flux o Received by Stream represents the solar heat flux that enters the water column after accounting for the surface reflection transmission through the water column and substrate absorption Page 129 Chapter IV Model Operation Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Chart Solar Flux Worksheet Select Stream KM to Plot Energy Balance Diel Solar Heat Flux Profile for River KM 39 34 Effective Shade 86 Solar Radiation W m2 Directly Received VARA AN a 14 9912 00AM 0 00 0 00 0 00 8 14 99 2 00AM 000 0 00 0 00 PER E AE 8 14 99 4 00AM 0 00 0 00 0 00 8 14 99 6 00AM 709 0 79 052 9 14 99 8 00AM 338 29 8 49 557 6 14 99 10 00 AM 675 03 237 84 157 10 6 14 99 12 00 PM 669 88 216 63 146 11 eae 8 14 99 2 00 PM 859 21 1338 12 78 8 14 99 4 00 PM 646 2 20 78 13 64 E WSIS 8 14 99 6 00 PM 300 90 8 37 J 6 14 99 8 00 PM 0 00 0 00 6 14 99 10 00 PM 0 00 6 15 99 12 00 AM 0 00 8 15 99 2 00 AM 0 00 yt i 8 15 99 4 00 AM i 0 00 8 15 99 6 00 AM 0 64 6 15 99 8 00 AM i 8 39 8 15 99 10 00 AM fa coral 6 15 99 12 00 PM 8 216 19 8 15 99 2 00 PM 19 01 8 15 99 4 00 PM ae 20 39 6 15 99
206. r returns to the stream system at some down gradient location For example diversions route water over varying distances in canals and irrigation systems causing an immediate decrease in instream flow volume A secondary effect is that the portion of irrigation flows returned to the stream system is often very warm further increasing instream temperatures Remotely sensed TIR stream temperature data is particularly suited to detecting these warmed return flows Other important considerations include altered instream hydraulics and wetted channel dimensions Flow velocity and travel times are highly related to flow volume Reduced flow velocity will translate to reduced shear stress and dispersion which result in obvious changes water column mixing A well mixed stream segment may become poorly mixed or stratified when flow volumes and corresponding flow velocities are reduced from instream withdrawals or natural low flow conditions The thermal assimilative capacity refers to an amount of heat a water column can receive to meat a desired condition i e temperature Page 19 Chapter Introduction Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 1 2 2 POINT SOURCES OF STREAM WARMING Thermal Infrared Multi Spectral Image with Color bap Mutti spectral Image Water in Thermal Infrared soe m IFL ee aa Et x Flaw Director b M N HE i N 7
207. r temperature and humidity Each expression typically has unique data constraint and are developed for specific applications and regions The mass transfer evaporation rate method is available for use in the model methodology Mass Transfer Evaporation Rate Dingman 2002 E f W fe e 2 96 Saturation Vapor Pressure Using Stream Temperature modified for units from Chapra 1997 1727 Ta paa 7 e 6 1275 e Vapor Pressure Based on Saturation Vapor Pressure Using Stream Temperature Bedient and Huber 1992 2 97 H 62 es 2 98 100 Wind Function t W is described in detail in following section Wind Functions ENERGY BUDGET METHOD The energy budget method calculates the evaporation rate as a function of heat transfer processes It is the most accurate and complex method for estimating evaporation dynamics Bedient and Huber 1992 As would be expected application of this method requires accurate measurements of free water surface temperature radiation attenuation and emission Atmospheric data also must be detailed and highly accurate and is considered a serious limitation of application of this method Bedient and Huber 1992 Despite these limitations the energy budget evaporation rate method is a widely used methodology However the calculated evaporation rate is a function of surface water temperature which is often an estimated or simulated condition A feedback mechanism resulting from errors in
208. ration Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 volume and water column depth An over prediction of the diurnal temperature change indicates that either too much heat transfer to the water column or that the flow rate and or water column depths are too low Similarly an under prediction of the diurnal temperature change indicates that either too little heat is transferred to the water column or that the flow rate and or water column depth are too large 4 7 DIALOGUE WINDOWS PURPOSE AND MEANING Many dialogue windows and message boxes will appear to help the user make decisions or explain problems While the meaning is likely fairly clear the purpose for these windows is explained briefly below 4 7 1 PROGRESS WINDOW There is a standard progress bar window that will appear during all model processes that take time to complete Features of the progress bar window include the title of the procedure the specific executable that is running the specific process of the executable and finally the progress of the process measured in terms of percentage competed Simulation Progress x Executable Heat Source Process Checking Morphology Data Sheet Pb AB 4 7 2 MESSAGE BOXES CLEARING INPUT DATA The user will be asked before operations that delete or change model inputs Now is a good time to suggest that the users save the model frequently a
209. rations offer significant advancements in stream temperature analysis RIVERS AND STREAMS ARE THERMALLY UNIQUE A definition of stream temperature uniqueness recognizes that the longitudinal temperature profile as well as spatial and temporal dynamics defined at virtually any scale applies only to one stream river or network Recently published literature is offering the scientific community evidence that stream and river systems are not only hydrologically and thermally unique but also complex Boyd M and B Kasper 2002 Faux et al 2001 Torgersen et al 2001 Torgersen et al 1999 Torgersen et al 1995 Stream temperature distributions are highly characteristic of individual stream river reaches and these unique temperature patterns are expressed inter annually An example of unique thermal patterns between similar streams can be found in the North and South Forks of the Sprague River Thermal infrared radiometry TIR measured stream temperature data suggest that the North and South Forks of the Sprague River exhibit temperature dynamics specific to each stream across multiple scales Both stream have similar summertime low flows of 0 85 cms 30 cfs and originate from similar sized drainages with similar topography geology and land use patterns TIR sampling occurred within the same period of the day 4 00 PM on August 12 and August 16 1999 see Figure 1 1 Despite these apparent similarities each stream exhibits different stream temp
210. ream riparian orientation Near stream land cover height width and density describe the physical barriers between the stream and sun that can attenuate and scatter incoming solar radiation i e produce shade The solar position has a vertical component i e solar altitude and a horizontal component i e solar azimuth that are both functions of time date i e solar declination and the earth s rotation i e hour angle measured as 15 per hour While the interaction of these shade variables may seem complex the mathematics that describes them is relatively straightforward geometry see Figure 1 2 Using solar tables or mathematical simulations the potential daily solar load can be quantified The measured solar load at the stream surface can easily be measured with a Solar Pathfinder hemispherical canopy photography or estimated using mathematical shade simulation computer programs Boyd 1996 Chen 1994 Park 1993 Page 13 Chapter Introduction Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Effective Shade Defined solar Potential daily direct beam solar radiation load adjusted for julian day solar altitude solar azimuth and site elevation Solar Solar Effective Shade Solar Where Solar Potential Daily Direct Beam Solar Radiation Load solar Daily Direct Beam Solar Radiation Load Received at the Stream Surfac
211. responds to increased rates of stream temperature heating while moderate increases in effective shade correspond to lower rates of stream heating see Figure 1 4 While we should always start discussions of stream temperature with an acknowledgement of complexity simply matching observed measured thermal responses to theoretical science can serve as a powerful method of assessment Poor shade results from near stream vegetation removal and is compounded by channel morphology response to near stream vegetation removal Vey Meadow Grande Ronde River Oregon Page 16 Chapter Introduction Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 With this context the TIR and instream temperature data was collected for the Grande Ronde River on August 4 1999 From the TIR data flown around 4 00 PM it is apparent that stream temperatures are warmer at the end of the meadow by roughly 3 C where shade levels are very low near zero when compared to the upstream temperatures entering the meadow Stream heating is moderated by increased shade levels 20 to 40 in the forested downstream reach Further a close inspection of the graph reveals corresponding cooler temperatures associated with minor increases in shade levels This observation fits well with the accepted body of science the literature supports the theory that shade has a moderating effect upon stream
212. rial Photos e Map Roads Development Structures Measure Surface Water Temperatures Develop Longitudinal Temperature Profiles Identify Subsurface Hydrology Groundwater Inflow Thermal Infrared Radiometry Temperature Data TIR Springs D pan a g gt c a ni 2 s 5 rf 5 D G6 gt O oo g a Ss lt oo gt oD DQ oD O 0 a Ww G 2 o Oo o 56 0 D E gt ay al N N PTS E J Horizontal amp 5 6 E DBD F O lt O am X O Q O TE Map Scale Accuracy 1 50 000 82 0 feet oo T 1 24 000 40 1feet WE fT 1 20 000_ 33 4feet MMMM TE o o 15 000 84feet of 1 2 000 35feett 11 000 175fet Recommended Map Scale amp Horizontal Accuracy FIGURE 5 1 Widely Available Spatial Data Types and the Associated Resolution Page 140 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 5 3 AERIAL IMAGERY DIGITAL ORTHOPHOTO QUADRANGLES AND RECTIFIED AERIAL PHOTOS Spatial data sets derived from Aerial Imagery include e Stream Position e Stream Aspect e Channel Width e Near Stream Riparian Land Cover A digital orthophoto quadrangle DOQ is a digital aerial photograph in which displacements caused by the camera angle and the terrain have been removed It combines the image characteristics of a phot
213. ric Composite Heat Capacity in Conduction Layer V Vh o CoL C es T nc V Coed 1 n Cno n 2 86 CL CL Volumetric Composite Density in Conduction Layer V Vh o Pot Z Pno E Psa 1 n Pno n 2 87 CL CL Volumetric Composite Thermal Diffusivity in Conduction Layer V V0 Qc a Yen A ano z a sea 1 7 n lano n 2 88 CL VeL Conduction Layer Depth d 0 2 m 2 89 Substrate Conduction Flux with Water Column A E Ta conduction Pct cr cL Tou Tw Ko Mau Tw 2 90 OG Or 2 2 Substrate Conduction Flux with Alluvium l ed a E AAA por Cor io Meu Taun Key Camin Tx 2 91 Och CoL 2 2 Change in Conduction Layer Temperature from Heat Transfer 2 alluvium Ac dt Afc lo SR7 p conduction p conduction V CL Pct CoL alluvium P dx dt lo SR7 7 D conduction 2 conduction l A E lluvi dt o ak7 conduction conduction ETE TA 2 92 CL Pcl CoL Conduction Layer Temperature a oe F Alo 2 93 Page 56 Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Variables Measured Known dso Substrate particle size mm ds2 7 _ Fine sediment particle size 0 062 mm dx Stream segment length m E Embeddedness unitless Cg Substrate Specific Heat Capacity 2219 mare cho Water Specific Heat Capacity 4187 T Oseq
214. rksheet are Flow Volume cms Flow Velocity m s Wetted Width m Average Wetted Depth m Maximum Wetted Depth m Hyporheic Exchange Volume cms Tendency to Stratify via Densiometric Froude Number OUTPUT TEMPERATURE Page 131 Hourly water temperature output data are listed in the Output Temperature worksheet Chapter IV Model Operation Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 OUTPUT SOLAR POTENTIAL Hourly solar heat flux both diffuse and direct beam data that would reach the stream surface without shading or obstructions of any kind attenuate or scatter shortwave radiation i e without land cover topography stream banks etc Cloudiness is accounted for in the Potential solar heat flux OUTPUT SOLAR SURFACE Hourly solar heat flux output data that reaches the stream surface with shading and obstructions that attenuate and scatter shortwave radiation i e with land cover topography stream banks etc Cloudiness is accounted for in the Directly Above Stream solar heat flux OUTPUT SOLAR RECEIVED Hourly solar heat flux output data that enters the water column after accounting for the surface reflection transmission through the water column and substrate absorption OUTPUT SOLAR LONGWAVE Hourly longwave thermal radiation heat flux output data that accounts for atmospheric and land cover sour
215. rom Dispersion 2 wep Tw 2 114 OX The dispersion coefficient D_ may be calculated by stream dimensions roughness and flow Fischer et al 1979 For streams that exhibit high flow velocities and low longitudinal temperature gradients it may be assumed that the 12 See Chapter 3 for a detailed description of advection 13 See Chapter 3 for a detailed description of dispersion Page 65 Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 system is advection dominated and the dispersion coefficient may approach zero Sinokrot and Stefan 1993 Regardless dispersion is included in the simulation methodology The longitudinal dispersion coefficient is determined from stream dimensions and flow velocity with a relationship developed by Fischer et al 1979 Physical Dispersion Coefficient Fischer et al 1979 Dy 0 01 2 115 U dw Shear velocities result from the frictional forces exerted upon flowing water at the substrate boundary Most formulations of shear velocity are based upon representations of shear stress Martin and McCutcheon 1999 Shear Stress as a Function of Slope and Water Column Depth Martin and McCutcheon 1999 T ppo 9 dw S 2 116 Shear Velocity as a Function of Shear Stress Martin and McCutcheon 1999 U g dw S 2 117 PHO The simultaneous non uniform one dimensional tr
216. rom the water column when substrate temperatures are less than the water column temperatures In essence the conduction layer represents a heat buffer with the stream and does so as a function of temperature differences between the water and substrate particle size embeddedness and channel geometry Sediment Thermal Conductivity Potter and Wiggert 1991 K sed Psed Csed sed 2 79 1600 2 2219 0 0000045 15 977 m kg C s m s C Water Thermal Conductivity Potter and Wiggert 1991 Kho PHO CH 0 H 0 2 80 1000 lt 2 4187 0 0000001433 1 0 600 m kg C S m s C Variables Used in Thermal Conductivity Calculations Density Psed 16005 Pho 1000 4 Thermal Diffusivity Oseq 0 0000045 ayy 5 0 0000001433 1 Specific Heat Capacity Coog 2219 ae Cpo 4187 J kg C Conduction Layer Assumes 100 Particles Thickness cL ea 0 1 m lt dso lt 0 3 m 2 81 Sediment Volume in Conduction Layer Vseq 1 n Pw dor dx 2 82 Water Volume in Conduction Layer Vio n Pw do dx 2 83 Total Volume in Conduction Layer VeL Pw dc dx 2 84 Volumetric Composite Thermal Conductivity in Conduction Layer V V Kol Kea Ve t Kuo A K sea l 1 gt n Kuo n 2 85 L L Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Volumet
217. s Measured Known dx Model Distance Step m Calculated E Evaporation Rate Qevap Evaporation Loss Rate 2 Ww Wetted Width m Page 97 Chapter IIl Dynamic Mass Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 3 5 FLOW VOLUME CONTINUITY Mass transfer to and from the water column coupled with dynamic flow routing makes it possible to account for volumes of water at any time t and location model node i Inflows 2 2in are the summation of surface tributary flows subsurface springs seeps and accretion flows and hyporheic flow Flow losses 2 Qour are simply the summation of withdrawal rates and evaporation losses The flow rate Qt presented in 3 44 is calculated from the dynamic flow routing methods discussed in Section 3 2 Instantaneous Summation of Inflows Qni gt Qrrei X Qew Crna m G 3 41 Instantaneous Summation of Outflows Qourti gt Qwithi t ayap 3 42 Instantaneous Model Reach Volume When Flow Rate Q _ is Known Vwi at Qni Qouri dt 3 43 Instantaneous Model Reach Volume When Flow Rate Q is Unknown Vwi Q Qni Z Goya dt 3 44 Variables Measured Known dt Model Time Step s Calculated Q Flow Rate 2 Qevap Evaporation Loss Rate m2 Qew Instantaneous Flow Summation of Subsurface Inflows Qhyp Hyporheic Exchange Rate Across Seepage Face
218. s Now consider that data collection methods are not available to quantify this variability Consequently such complexity variability and interdependence is not easily accounted for in most analytical methods at least in a practical sense Further even if algorithms are developed to simulate these processes validation of model performance will be difficult due to the aforementioned data and instrumentation limitations along with methodology limitations The result is that microclimates are not included in stream temperature analysis in a complete fashion Changes in rates of heat transfer can vary considerably across relatively small spatial and temporal scales In quantifying and understanding stream heat and mass transfer processes the challenge is not represented in theoretical conceptions of thermodynamics and relations to flowing water Thermodynamics is a well established academic discipline that offers a scientifically tested methodology for understanding stream temperature In fact the methodology used to evaluate stream temperature is quite simple when compared to other thermodynamic applications that have become common technological necessities to the American way of life i e a car radiators cooling towers solar thermal panels insulation etc Instead the true challenge in understanding stream temperature materializes with the recognition that thermally significant heat and mass transfer processes occur in very fine spatial and t
219. s The actual Sampling procedure is consistent time after time and the results are as good as the geospatial data sets that are sampled Page 139 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 5 2 GEOSPATIAL DATA OVERVIEW TTools is designed to sample high resolution spatial data sets Several GIS data sources that can be used are listed in Table 5 1 Developing spatial data sets from existing GIS or remotely sensed data must consider data resolution map scale and positional accuracy GIS data sources that describe landscape parameters can be developed at a high resolution i e less than 1 5 000 however many of the existing spatial data sets are coarse and may fail to capture variable landscape parameters Modules contained in TTools can employ high resolution sampling provided that high resolution 1 5 000 spatial data sets are available It should be noted that the sampling density is user defined and should be scaled to match GIS data resolution accuracy Table 5 1 Spatial Data Types and Applications Spatial Data Application Digital Elevation Model Measure Valley Morphology DEM e Measure Topographic Shade Angles l e Measure Stream Elevations and Gradients Aerial Imagery e Map Streams 1 5 000 scale Digital Orthophoto e Map Near Stream Vegetation 1 5 000 scale Quadrangles and e Map Channel Morphology Rectified Ae
220. s Transfer Methodology for the Heat Source Model Version 7 0 Second Approximation t 1 of the Slope MacCormick 1969 t 1 t 1 wit twin S2t k dx t 1 t 1 t 1 Twie 2 Twi Twig D i dx t 1 a o total 2 1 D Pho Ch o dw Backward Second Approximation t for Final Predictor Calculation MacCormick 1969 Sa tS i h 4 Fu sat dt 2 122 Variables Measured Known Cho Specific Heat of Water dx Model Distance Step m Pho Density of Water 998 2 Lo m x Longitudinal Distance m t Time s Calculated D_ Dispersion Coefficient dw Average Water Column Depth m Divar Total Heat Flux 7 Sit Sor Approximation of the Slope Tw Water Temperature C U Average Flow Velocity Boundary conditions are defined for the finite difference solution and displayed in Figure 2 7 The temperatures at the upstream boundary io for all time steps to t 1 t t 1 are supplied by hourly temperature data inputs It is assumed at the downstream boundary position x in Figure 2 7 that temperature remains constant with respect to time Initial values of the temperatures at each distance node i I 1 1 1 1 occurring at the starting time t are equal to the boundary condition at time t The initial condition of the model is quite irrelevant since model convergence should be independent of the initial condition However convergence will occur faster when the initial condit
221. s that you created FIGURE 5 15 Example of Delete the Overlapping Lines and the Splice Lines Page 162 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 5 7 3 CLEANING THE UNDERSHOOTS Undershoots may occur during the digitizing process if you had forgotten to turn on the snapping feature or if you did not start a new line close enough to an old line Undershoots also are an intermediate product of cleaning an overshoot i e once you splice out the overshoot segments you are left with an undershoot that still needs to be fixed 1 Make sure that your stream theme is the edit mode Theme Start Editing 2 Click on the Interactive Snapping Tool on the tool bar It looks like this If the Snapping Tool button is not visible then go to Theme Properties In the pop up window select the Editing icon on the left Check both the interactive and general snapping boxes Click OK 3 Now use the cursor to draw a Snapping radius around one of the loose ends SI ZINTA ease E kacak Center 013 00 Flodus Uitm 4 Click on the Draw Line button in the tool bar It looks like this S 5 Draw a line that connects the two loose ends You should see your snapping radius circles appear as your are drawing the connection line You know you are done cleaning when A You zoom out to the full ext
222. sponding time step of one minute Model time and distance steps are left to the user s discretion These finite difference steps are used for all finite element methods Heat and Mass Transfer Dynamic Flow Routing and thus have multiple stability criteria Familiarity with the methods and the analytical needs of the user are fundamental to the selection of appropriate time and distance steps As a basic rule the distance step should always be equal to or greater than the longitudinal spatial data sampling rate used in TTools Keep in mind that the longitudinal spatial data sampling rate used in T Tools should always be equal to or greater than the data resolution including horizontal accuracy Time and distance steps are interrelated and changes in one will affect the limits applied to the other While changes in time and distance steps should not significantly affect mathematically simulation results other effects may manifest altered simulation results Heat Source averages spatial data inputs between finite difference nodes as determined by the selected distance step Therefore a large distance step relative to the sampling step will reduce data resolution and spatial accuracy simply by averaging the uniqueness and variability Further a larger distance step often requires a large corresponding time step which decreases model temporal resolution Ultimately the selection of time and distance steps is left to the user s discretio
223. ss Transfer Methodology for the Heat Source Model Version 7 0 Variables Measured Known Oat Latitude degrees Calculated a Atmospheric Elevation degrees Cr Refraction Coefficient degrees Solar Declination degrees Oaz Solar Azimuth degrees Qua Hour Angle degrees Osa Solar Altitude degrees Osz Solar Zenith Uncorrected degrees Osz Solar Zenith Corrected degrees 2 2 4 SOLAR RADIATION HEAT ABOVE TOPOGRAPHIC FEATURES Once emitted from the sun photons travel through space to the outer edge of the atmosphere at an average vertical intensity referred to as the solar constant The solar constant is approximately 1367 W m Dingman 2002 The radius vector r is the ratio of the actual distance to the mean distance between the Earth and sun and is required for the calculation of extraterrestrial global solar radiation spo Global Solar Radiation Flux at the Edge of the Atmosphere Wunderlich 1972 D spre 2 SiN Osa 2 26 Solar Constant Dingman 2002 Dopc 1367 2 27 m Radius Vector Wunderlich 1972 r 1 0 017 Cos 2 2 186 u0 t281 2 28 While passing through the atmosphere solar radiation is absorbed and scattered by ozone water vapor dry air and particulate McCutcheon 1989 The flux of direct beam solar radiation that traverses the atmospheric air mass must account for attenuation and scattering induced by atmospheric transmissivity T and cloudiness C along a
224. ssacson E J J Stoker and B A Troesch 1956 Numerical solutionof flood prediction and river regulation problems Inst Math Sci Report No IMM 235 New York University New York Jerlov W G 1976 Marine optics Elsevier Scient Publ Comp Elseveir Oceanography Series 14 231 p Jobson H E and T N Keefer 1979 Modeling highly transient flow mass and heat transfer in the Chattahoochee River near Atlanta Georgia Geological Survey Professional Paper 1136 U S Gov Printing Office Washington D C Kay J Allen T Fraser R Luvall J Ulanowicz R 2001 Can we use energy based indicators to characterize and measure the status of ecosystems human disturbed and natural in Ulgiati S Brown M T Giampietro M Herendeen R Mayumi K eds Proceedings of the international workshop Advances in Energy Studies exploring supplies constraints and strategies Porto Venere Italy 23 27 May 2000 pp 121 133 Kovalchik B L 1987 Riparian zone associations R6 ECOL TP 279 87 USDA Forest Service Pacific Northwest Region Kustas W P A Rango and R Uijlenhoet 1994 A simple energy balance algorithm for snowmelt runoff model Water Resources Research 30 1515 1527 Leopold L B M G Wolman and J P Miller 1964 Fluvial Processes in Geomorphology Freeman San Francisco California 522 pp MacCormick R W 1969 The effect of viscosity in hypervelocity impact cratering Am Inst Aeronaut Astronaut Pap
225. surement is performed in 90 intervals for the 360 representing all solar azimuth angles i e west south and east The topographic shade angle that is closest to the solar azimuth is used in the model to determine whether topographic shade is occurring Page 40 Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Variables Measured Known 0t Topographic Shade Angle West degrees T Topographic Shade Angle South degrees T Topographic Shade Angle East degrees Calculated sprg Direct Beam Solar Radiation above Topography 2 sprp Diffuse Solar Radiation above Topography Gee sprg Direct Beam Solar Radiation below Topography a srpo Diffuse Solar Radiation below Topography z 2 2 6 SOLAR RADIATION HEAT BELOW LAND COVER Land cover physical attributes height overhanging distance and density are used as model inputs These data are sampled using T Tools in four consecutive zones for seven directions northeast east southeast south southwest west northwest Direct beam and diffuse solar radiation is routed through these land cover zones and canopy openings Direct beam radiation is routed through land cover zones in the direction i e southwest aspect 225 closest to the solar azimuth i e solar azimuth 231 Routing occurs from the outermost land cover zone zone 4 to the innermos
226. t Affect Stream Important thermal parameters Temperature that are highly sensitive to human activities and that significantly affect the stream temperature regime include Effective Shade Controlled by near stream vegetation and channel morphology Hydrology eFlow Volume Regime Shear Velocity Point Sources Withdrawals Augmentation Hyporheic Flows Sedimentation Stream Flow Controlled by withdrawals augmentation and discharge from point sources The following subsections expand upon the role of effective shade and flow volume in recognition that these two parameters are often implicated in human caused stream temperature modifications LAND COVER MORPHOLOGY AND EFFECTIVE SHADE The solar radiation heat process considered in the stream thermal budget is often the most significant heat transfer process and can be highly influenced by human related activity Decreased levels of stream shade increase solar radiation loading to a stream The primary factors that determine stream surface shade are near stream land cover type and associated physical characteristics and channel morphology Near stream land cover height controls the shadow length cast across the stream surface and the timing of the shadow Channel width determines the shadow length necessary to shade the stream surface Near stream land cover and channel morphology are often interrelated Stream bank erosion rates are often a
227. t by the user or restored by hitting the default button Important e Many wind function coefficients are Data Sheets Evaporation Rate Methods available in the came Mass Transfer Dalton Type Continuous Data simple method that predicts the adiabatic energy associated with literature Info General Model Input Model Setup Executables Diagrams evaporation e Make sure that you Combination Method Penman have correctly aik A more complex method that predicts the adiabatic and diabatic accounted for the energy associated with evaporation Associate Ww D Evaporation Rate Models Wind Function units a mb 1m s 1 a l 0 000000001505 and b mb 1 _Eankful Morph i Penman Evaporation Rate b o ooo0000016 V Include Evaporation Losses Defualts Bed Conduction if evaporation losses are included all data found on all input sheets see Table 2 3 for Yema Mass Transfer Data dea hea Required for Heat Source and Flow Router if evap is included Flow Routing are required Function Coefficients r am Asoraonate model use tt seer be at and apolication are the Bingo Sit tiene sole responsiblity of fhe Oregon user Department of SM Ae a ree Environmental k i Hide Main Menu i Sr a Page 118 Chapter IV Model Operation Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 4 3 9 MODEL SETUP STREAM BED CONDU
228. t zone zone 1 Page 41 Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Shadows that are cast from each land cover zone are calculated as a function of solar altitude and azimuth in addition to the physical attributes of the land cover and terrain elevation If the shadow length spans the width of the stream then the stream is shaded This methodology is based on simulation of the sun gt stream vector and it follows that positional information for both the sun and stream require highly accurate description and analytical methodology When stream surface shade is determined to be occurring direct beam attenuation occurs as a function of a light extinction coefficient and the path length through the land cover zone The path length through the land cover zone is a function of zone width stream aspect solar altitude and solar azimuth Attenuation is calculated using Beer s Law Oke 1978 Direct beam radiant energy that passes through Model a land cover zone is then Node routed to the next inner jet land cover zone and the process is repeated Once E F through all four land cover Directional zones the remaining direct pane beam solar radiation is iie Samples routed to the stream bank elevation Position 4 i a ta E t Diffuse solar radiation eres filters through the openings neste in land cover and is
229. tcheon 1989 The total longwave radiation flux is simply the instantaneous summation of the positive longwave radiation flux atmospheric and land cover and the negative longwave radiation flux back radiation Longwave Radiation Flux Attenuated in Water Column Longwave Continuity P longwave Diw DEW Diw 2 73 Atmospheric Longwave Radiation Flux Attenuated in Water Column McCutcheon 1989 Oh 0 96 Eam 0 Ta 273 2 2 74 Land Cover Longwave Radiation Flux Attenuated in Water Column adopted frm McCutcheon 1989 DLG 0 96 1 Oyrs 0 96 o T 273 27 2 75 Longwave Radiation Flux Emitted from Water Column Back Radiation adopted from McCutcheon 1989 DSy 0 96 o Tw 273 27 2 76 Atmospheric Emissivity Dingman 2002 Kustas et al 1994 1 0 1 e 7 2 4 72 8a _ 449 2246 2 77 atm z Tee L aes Vapor Pressure Bedient and Huber 1992 H e e 2 8 a 100 G Page 51 Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Saturation Vapor Pressure modified from Chapra 1997 and Raudkivi 1979 17 27 T e 6 1275 e 9th 2 79 80 Humidity 100 Q 75 3 FIGURE 2 4 os Calculated Vapor a g 50 Pressure e Values a Calculated from gt Equations 2 78 and 2 79 25 0 5 10 15 20 2 30 35 40 Air Temperature C Variables Measur
230. te dynamic open channel hydraulics flow routing heat transfer effective shade and stream temperature This documentation is developed to support Heat Source version 7 0 Page 1 Chapter Introduction Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Methods for spatial data derivation have been developed and packaged as an ArcView version 3 0 or higher extension and is referred to as TTools The sampling methods within TTools allow for continuous measurements of channel morphology land cover and topography Spatial data derivations sampled and calculated by TTools are then imported into Heat Source as data inputs Heat Source consists of a Microsoft Excel version 2000 or higher spreadsheet that contains model input and output No calculations are made in the spreadsheet itself Instead Visual Basic programming computes all dynamic mass and heat transfer simulation algorithms Modules executables include simulation of effective shade comprehensive heat and mass transfer and water temperature these modules along with setup routines are controlled from a central Main Menu 1 1 1 THE STATE OF THE SCIENCE The models used for stream temperature prediction are becoming standardized and widely available However data availability and the increased ease of monitoring coupled with aerial imagery GIS data and remote sensing and finally model operation conside
231. temperature simulation may create errors in evaporation simulation with a compounding effect Lastly unlike the other two evaporation simulation methods presented in this section there are not calibration parameters a and b and results cannot be calibrated by the user Page 60 Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Energy Budget Evaporation Rate Dingman 2002 solar T P longwave i conduction T Dam P aa Eo PH 0 Le 1 Bp aa Water Advected Heat Dingman 2002 Pam n Qin Tn Qew Tew Qour Tour 2 100 Change in Stored Heat Dingman 2002 Paa PEE THS ha Tw Q Tw 2 101 Bowen s Ratio of Sensible Heat to Evaporative Heat modified for units from Bedient and Huber 1992 Twi T Ba 0 00061 P i_ 2 102 es ey Adiabatic Air Pressure Dingman 2002 Pa 1013 0 1055 z 2 103 COMBINATION METHOD PENMAN Penman 1948 developed a combination method to capture both the mass transfer and the energy budget components involved in estimating evaporation rates This method does not require surface water temperatures which represents a considerable improvement over the energy budget method Further heat energy terms are included extending the simulation to diabatic vaporization processes as well as the mass transfer adiabatic aerodynamic processes The Penman method is widely used si
232. ter column is a function path length PLw and the transmissivity Ty of the water column which in turn are calculated from the solar angle 8s and average water depth dw Solar radiation is received at the stream bed and absorbed as a function of solar angle and literature values for reflectivity properties of quartz Beschta and Weatherred 1984 Heat absorbed by the streambed will cause differential heating and become part of the substrate lt owater column conduction pathway The remaining portion of solar direct beam radiation is reflected from the stream bed and travels towards the surface of the water column where again there is absorption of solar radiation as a function of path length and stream transmissivity Page 47 Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Solar Radiation Flux Attenuated in Water Column P solar Psre Psrge Psrve 2 50 Solar Radiation Flux Attenuated in Stream Bed Psr7 Psrg7 Psrpv7z 2 51 DIRECT BEAM SOLAR RADIATION ROUTING THROUGH WATER COLUMN Direct Beam Solar Radiation Water Column Path Length Jerlov 1976 Pyne 2 52 Sinl 0 Z S2 180 1 333 Cosl Sin Transmissivity of Water for Direct Beam Solar Radiation Austin and Halikas 1976 TR 0 415 0 194 Log4o PL w 2 53 Stream Bed Reflectivity Beschta and Weathered 1984 adopted from Sellers 1965
233. tered microclimates and flow modifications Legacy morphology conditions and land cover distributions can sometimes be caused by natural disturbances Overall the extent of natural disturbances on near stream land cover channel morphology and hydrology is not well documented and complicated by geologic time scales Factors that cool streams and rivers that are of non human origin can be broken into mass and heat transfer sources Conditions that reduce radiant heat exposure will prevent or reduce rates of stream heating and in some cases reduce stream heating rates and gradients Such conditions include the persistent effects of shade produced from riparian vegetation stream surface area reduction via healthy equilibrium morphology and cool near stream microclimates that occur in well vegetated riparian corridors There are also episodic cooling effects that reduce radiant heat exposure such as cloudiness or any other form of vapor and particulate matter in the overlaying air mass and cool air temperatures that reduce thermal radiation emission from the atmosphere vegetation and topography that is received by a stream Natural mass transfers of inflow tributaries springs etc can obviously heat and cool the receiving water Typically subsurface water is cooler than surface water Cooler subsurface waters tend to come from deeper ground water sources and snowmelt sources Shallow groundwater and hyporheic flows typically have warmer temperatur
234. the Heat Source Model Version 7 0 4 3 5 MODEL SETUP TTOOLS DATA The data in the TTools database file is formatted to be simply copied and pasted into the appropriate TTools Data worksheet columns Starting with longitude column F the columns are arranged in the same order so that multiple columns of data can be inserted copied and pasted directly from the TTools derived dbf tile After you have inserted the data scroll down to the bottom of data set and check to see that the data row count matches the longitudinal row count red font color columns B gt E Important To minimize spreadsheet bloat you should copy only the cells that have data and then paste special values into Heat Source If you choose to numerically format the cells on this page keep in mind that you will increase the spreadsheet file size TTools Data Worksheet Enter Sampled TTools Data gt Topo Shade dec z Heat Long Ta 9 Source Distance z a z r Node km Stream km Ww oO 51 54 0 05 51 49 0 1 51 44 0 15 51 39 O 2 51 34 E W M Oo 4 3 6 MODEL SETUP LAND COVER CODES AND ATTRIBUTE ASSOCIATIONS The TTools Data worksheet should now contain all of the TTools data A portion of these data are the sampled land cover classifications The Land Cover Codes worksheet will contain the physical attribute information associated with each classification Data entry is fairly straightforward Land cove
235. this new line theme and make it easier to see That is change the line width from 0 1 to 2 and make the color something that will show up against the aerial imagery 6 Goto Theme Properties Select the Editing button on the left side of the dialog box Under Snapping check the boxes next to both General and Interactive and in each of the Tolerance dialog boxes Then click OK to get out of this dialog box 9 Now click on the Interactive Snap tool which appears in your Toolbar as follows 10 Now right mouse click in EE i 3S Is OEE the view holding the Ea 28 AS 233525 DO ee button down and this Se 2283 Fe WWE will create a circle Snapping radius around your cursor This will help you connect the ends of two lines by making sure that the end of a previously drawn line is within the circle when you start the new line g Thi Cerniex 0 79 069 m Aadi MOS m D Page 158 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 11 Select the Draw Line tool which looks like 12 Beginning at the mouth of the stream start tracing the center of the wetted channel 13 Click whenever the stream channel makes a bend since you can t draw curves with your mouse 14 When you get close to the edge of the screen frame right mouse click and select Pan Th
236. transfer processes and mass transfer processes To isolate the human influence on this expression it is important to associate the human influence on the heat transfer processes and or mass transfer processes Effective shade is consistently identified in the literature as an important thermal control that is often influenced by human activity The combined effect of land cover physical attributes and channel morphology control the timing and extent of effective shade cast upon the stream surface It is important to consider that land cover type and condition affects and is affected by channel morphology bank stability shallow ground water characteristics riparian nutrient cycles aerobic or anaerobic rooting conditions etc A meaningful assessment of effective shade should include both land cover and morphologic spatial data and analysis Flow volume is also an important thermodynamic and hydrologic parameter that is subject to obvious human manipulations Many parameters are affected by flow volume In fact the flow regime of a riverine system formulates the basic connectivity of instream and riparian processes The thermodynamic influences of the flow regime cannot be easily summarized simply because of the wide and diverse influences that flow has upon the thermal regime Page 9 Chapter Introduction Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Factors tha
237. tude describes the geocentric position as the Earth s mean equator and equinox of a standard epoch on the celestial sohere centered at the Sun A mean position is determined by removing the effects of refraction geocentric and Stellar parallax and stellar aberration from the directly observed position and by referring to the coordinates to the mean equator and equinox of a standard epoch The geometric mean of the longitude of the sun 6 is a function of time measured in Julian centuries tjpc Geometric Mean of the Longitude of the Sun 0 8 lt lt 360 Ozz 280 46646 typo 36000 7698 3 0 0003032 t jnc 2 9 The geocentric position of the anomaly 6 is an angular measurement of the Earth in its orbit from its perihelion the point at which the Earth most closely approaches the sun and is calculated as a function of time measured in Julian centuries tjpc Geometric Mean of Anomaly of the Sun degrees 075 357 52911 t jpc 35999 05029 0 0001537 tnc 2 10 Variables Calculated Ec Eccentricity of Earth s Orbit unitless 975 Geometric Mean of Anomaly of the Sun degrees 975 Geometric Mean of the Longitude of the Sun degrees 95s Mean Obliquity of the Elliptic degrees Oog Obliquity of the Elliptic degrees typc Julian centuries since epoch 1900 January 0 5 ET Page 32 Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Metho
238. ubsurface Inflows i Qewi e 3 36 i 1 Instantaneous Flow Weighted Temperature of Subsurface Inflows Sow Tg Tawi 3 37 Qay i GW i 1 Resulting Temperature after Complete Mix with Subsurface Inflows Twi Twi af Tow Qowi 3 38 Qi Qew Page 93 Chapter Ill Dynamic Mass Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Variables Measured Known dx Model Distance Step m Qaw Subsurface Inflow Flow Rate m Tew Subsurface Inflow Temperature C Calculated Q Flow Rate 1 gt Qew Instantaneous Flow Summation of Subsurface Inflows m2 Tew Instantaneous Flow Weighted Temperature of Subsurface Inflows C Tw Water Column Temperature C 3 4 5 HYPORHEIC FLOWS Hyporheic flows occur when surface water from a stream or river infiltrates into the alluvial aquifer and eventually travel back to the surface water column down gradient Poole and Berman 2001 Poole et al 2000 Alluvium comprised of depositional materials and substrate underlies the stream channel This material is sorted to some degree by tractive forces and shear stress associated with surface high flow conditions The distribution of alluvium can vary significantly within the channel and across the floodplain The supply of sediments and the flows patterns during peak flow events affect the distribution and type of sediment found in the al
239. unmapped and undocumented In such cases it becomes important to establish the direction of flow i e influent or effluent With the precision afforded by TIR sampled stream temperatures effluent flows can be determined when temperatures are the same Temperature differences indicate that the flow is influent This holds true even when observed Page 90 Chapter Ill Dynamic Mass Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 temperature differences are very small The rate of water loss from diversions or withdrawals cannot be easily calculated Oregon DEQ estimates water withdrawal flow rates from the water right information maintained by Oregon Water Resources Department OWRD A mass balance can be developed from relatively few instream measurements FLIR stream temperature data and water rights data Potential flow rates are easily calculated by removing all water withdrawals and agriculture return flows An example of a derived mass balance is presented in Figure 3 11 N F Sprague River 10 tributary inflows 6 agriculture related return flows 9 subsurface inflows 6 water withdrawals 31 Mass Transfer Processes 60 50 40 Potential Flow Volume y Flow Volume cfs OO O N O Current Flow Volume Measured Flow 10 0 l l l T T T T T T T T T T T T T T T T T T T T T T 30 25 20 15 10 5 0
240. ur riparian buffer polygon Name the output file This output file will become your working riparian vegetation map The new buffer is like a donut and there is one last step before it is ready for vegetation mapping 20 Zoom somewhere near the middle of the buffer 21 Go to Theme Start Editing 22 On the tool button bar select your polygon splicing tool it is a drop down button beneath the rectangle graphic button It looks like this 23 Now draw a line all the way across the middle of your buffer polygon theme Page 169 see image below This will separate the continuous donut polygon preparing it for the mapping process Be patient splitting may take a few minutes to appear in your view Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 O ArcView GIS Version 3 1 File Edit View Theme Analysis Surface Graphics aia or Help ese ae ZEEE Gra e e z 7 Seale 13202 120281815 DGIC ROE rai Union3 shp Uniont shp Splice Line Plygonishp Buffer 1 of Mierge2 Merge2 shp r Sycan_right_ogic s PA Sycan_leftogic shy Newfile shp Flirshp c Ttoob_data_ogicst e Right_bank_ogice sh iM Left_bank_ogicshp You now have a base polygon layer that will be used to map the riparian vegetation The following steps will get you started on the aerial imagery interpret
241. ured Known g Acceleration of Gravity 9 8 S Stream gradient unitless t Time s x Longitudinal Distance m Calculated dw Average Water Column Depth m 3 Q Flow Rate 2 S Storage m S Friction slope unitless U Average Flow Velocity S Page 77 Chapter IIl Dynamic Mass Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 3 3 2 MUSKINGUM CUNGE APPROXIMATION Conceptually the storage volume of water for any time t is the prism and the wedge storage of the stream segment i see Figure 3 4 The theoretical wedge that forms the basis for the Muskingum Method can occur in the upstream or downstream direction depending on whether flows are increasing Q gt Qi 1 or decreasing Q lt Q1 over the longitudinal distance A basic assumption of this method is that the cross sectional area A as defined by Manning s equation is proportional to flow rate for any give stream segment Such an assumption allows the volume storage S to become a function of discharge the ratio of storage to discharge K and a weighting factor X that controls the wedge height and thus the wedge storage that occurs in response to flow rate changes over a stream segment Cunge 1969 shows that the Muskingum expression represents the kinematic wave equation when the effects of diffusion are included The following derivation develops t
242. ures can be associated with location information and entered at a one hour interval It is important to differentiate between localized inflows and accretion flows see following subsections Inflow Data Sites refers to localized non accretion type flows such as tributaries springs returns point sources etc Double click on the number of inflow data sites from the list located in the Mass Transfer Data tab of the Main Menu This will trigger the automated setup of the Flow Data worksheet for localized inflow data with a time date interval of one hour The next step is to input the localized inflow positional information in columns I L This data associates a localized inflow to a point in the longitudinal stream length For each inflow data site you need to enter in columns O the time series inflow rates and inflow temperatures at a one hour interval for the entire Page 108 Chapter IV Model Operation Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 simulation period When inflows are close enough so that more than one occurs in a model distance step the inflow rates will be summed and a flow based average inflow temperature will be derived and used in the mixing calculations ACCRETION DISTRIBUTED FLOWS Accretion flows are inflows that enter the stream over more than one stream data node and typically are subsurface seeps th
243. ution of stream temperature can be plotted for any hour within the simulation period You will need to press Update List Box after each simulation run to populate the list box with the hourly data Chart Long Temp Worksheet SelectDate Time to Plot Longitudinal Temperatures 8 14 1999 Simulated Stream Temperature O 8 14 1999 2 00 00 AM 25 0 O 8 14 1999 4 00 00 AM 8 14 1999 6 00 00 AM i pdate List Box ae O00 Simulated C Stream Temp Qur KM C a 51 54 3 00 51 44 9 10 73 15 0 51 34 9 20 i 51 24 9 20 2 51 14 9 30 51 04 9 40 50 94 9 50 e 10 0 50 84 9 80 z 50 74 9 90 50 64 10 00 a 50 54 10 20 50 44 10 30 v 50 50 34 10 40 50 24 10 50 50 14 10 60 50 04 10 70 Plat Area 49 94 10 80 49 84 10 90 0 0 49 74 11 00 o 49 64 11 00 49 54 11 10 tO WU C9 N 49 44 11 30 49 34 11 30 Stream km 49 74 11 4n 4 5 4 CHART SOLAR FLUX The hourly simulated solar heat flux can be plotted for any river kilometer as determined by the model distance step by double clicking on the list box o Potential represents the solar heat flux both diffuse and direct beam that would reach the stream surface without shading or obstructions of any kind attenuate or scatter shortwave radiation i e without land cover topography stream banks etc Cloudiness is accounted for in the Potential solar heat flux o Directly Above Stream represents the sola
244. ve unwanted formatted or occupied cells is to delete them completely For this reason when Heat Source asks the user to delete or clear data from the worksheets the cells are in fact deleted TTools is designed to develop the spatial data inputs for Heat Source It is necessary to use T Tools to operate Heat Source in the fashion in which it is designed i e the use of multiple spatial data sets In particular the land cover information can only developed with the sampling routines contained in TTools The variability inherent to spatial data parameters warrants the measurement capability afforded by TTools Assuming such data is not an appropriate use of this methodology A utility program called the Land Cover Positioner is packaged with Heat Source to help users to reposition typical transverse land cover data i e left bank and right bank to the radial sampling pattern used by Heat Source Further the Land Cover Positioner also can be used to position land cover inputs following changes to the bankfull morphology i e bankfull width narrowing or widening Page 101 Chapter IV Model Operation Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 4 2 FINITE DIFFERENCE STEPS Important The distance step should always be equal to or greater than the longitudinal spatial data sampling rate used in TTools A typical distance step is 100 meters and with a corre
245. ved Mass Transfer Data longitudinal and transverse sampling A necessary first step is to set up the data sheets based on the stream length and database Vegematic sample rates You must press Setup Longitudinal Data before you enter any data into the worksheets Associate wD BankFull Morph eveper ation 1 You must setup the longitudinal data 7 Pede ondadon before you can enter land cover and Longitudinal morphology data required to run all of Flow Routing the executables TE Required for All Models Asoraonate model use ae ae at and apolicalion are the aa eee sole responsibility of fhe Oregon a wile T user Department of cs i es i J ce Environmental Quality ey ie i ae DEQ CE eg a 4 r _ ne hn A Pa Hide Main Menu am SE A message box will ask the user to confirm that they want to delete input data Configuring the longitudinal data involves changing location data in the model The user is asked whether they want to delete the current inputs associated with existing longitudinal data since these data are about to be changed If the user can keep track of existing data associations it may be easier to choose not to delete existing data and simple move it appropriately after the longitudinal setup configuration Heat Source Setup Longitudinal Data x x Do you want to clear existing data From the morphology and land cover input sheets ak Page 104 Chapter IV Model Operation
246. ver The uncorrected solar distance 0 7 is the angular distance on the Earth s sphere measured along the great circle from the zenith to the sun calculated as a function of solar declination 5 latitude 6 and hour angle 6 It may be easier to conceptualize the solar zenith as the angular distance 90 minus solar altitude The solar altitude is a measure of the angular distance of the sun above or below the horizon measured along the great circle passing through the Earth and the zenith angle And solar altitude is 90 minus the solar zenith angle Refraction refers to the change in direction of travel bending of a light ray as it passes obliquely through the atmosphere As a result of refraction the observed altitude of a celestial object is greater than its geometric altitude The amount of refraction depends on the altitude of the object and on atmospheric conditions The solar zenith and altitude comprise the vertical position of the sun relative to the stream segment Solar Zenith Corrected for Refraction Osz Osz Cp 2 20 Solar Altitude Corrected for Refraction Os 90 Osz 2 21 Solar Zenith Uncorrected for Refraction lbgal 1983 sz Cos A 2 22 TU where 1 lt A gt 1 A Sin Oa z sfs 180 180 Cos 0 Cos 5 27 Cog 0 480 180 A 180 Atmospheric Elevation Ibqal 1983 a 90 sz 2 23 Atmospheric elevation is simply the solar altitud
247. w routing is simulated as a function of derived spatial channel data geometry and slope and input values for channel roughness n and wedge storage X The numeric approximation is relatively efficient and stable even in highly varied flow regimes The methodology is fundamentally dependent on the assumption of wedge storage and travel time approximations Inherent to these approximations are Manning s based calculations that span time and distance steps for which it is assumed that flows are steady and uniform The duration of the time step may become a limiting factor if in fact flows vary over the course of any one time step The same concern also applies to the distance step However it is likely that finite difference mesh size will not pose these limiting factors when time and distance steps are small for example dt one minute dx 100 meters Page 84 Chapter Ill Dynamic Mass Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 The explicit finite difference method simulates storage of volume in stream segments and dynamic flow routing using an approximation that is based on the continuity and conservation of momentum equations In general the explicit method is used to simulate dynamic flows over well defined river reaches where channel data is robust Storage within a segment is completely dependent on channel bathometry and frictional forces Therefore
248. wever it is the author s opinion that most forms of model inaccuracy result from poor data input quality quantity rather than model algorithm error Users should consider that inaccurate model results may signal a problem with data inputs It is the experience of the authors that high resolution and accurate data inputs facilitate straight forward model operation and accurate simulation results 1 4 SALMONID LIFE STAGE THERMAL RANGES Salmonids and some amphibians are highly sensitive to temperature In particular bull trout Sa velinus confluentus are among the most temperature sensitive of the cold water fish species in the Pacifc Northwest Water temperature protective benchmarks usually employ logic that relies on using indicator species which are the most sensitive If temperatures are protective of indicator species other species will share in this level of protection lf water temperatures become too hot fish die almost instantaneously due to denaturing of critical enzyme systems in their bodies Hogan 1970 The ultimate instantaneous lethal limit occurs in high temperature ranges upper 90 F Such warm temperature extremes are rare natural aquatic systems More common and widespread are summertime water temperatures in the mid 70 F range mid to high 20 C range These temperatures cause death of cold water fish species during exposure times lasting a few hours to one day The exact temperature at which a cold water fish succum
249. width bankfull depth and average bankfull depth Select the Bankfull Morph tab from the Main Menu If the channel Channel Angle z is too large i e the channel sides converge then the morphology determined to resemble a V shape and the bankfull bottom width is zero Main Menu x Info General Model Input Model Setup Executables Diagrams Important e Make sure that you have entered stream Data Sheets Calculate Bankfull Morphology gradient banktull 3 Purpose Cont Dat width and channel _Continuous Data Select Calculate Banktull Morphology to derive the bottar width le bef Mass Transfer Data and channel depth channel dimensions SUPE ae EOE This step i dat G ted data will b d to devel YOU eal e step is mandatory Generated data will be used to develop Calculate Bankfull ydraulics PEN E Morphology button pankful Morph e You will be able to modify these inputs Evaporation later so do not spend You must calculate bankfull Calculate p Bed Conduction morphology hefore You can Bankfull 2 too much time on this F calculate hydraulics Morphology step right now Flow Routing ah Clear Sheets Asoraonate model use Bie d mmt and apolication are the ee e ee ni sole responsiblity of fhe Oregon as e USEF Department of 7 B a Tels ree Environmental wait eT Le DIX a a 4 T 7 ae z F ai Hide Main Menu a i Morphology Data W
250. y While shade is occurring there is still light penetrating to the stream derived from diffuse sources Shading algorithms mimic the travel direction of photons from the sun to the stream for both direct beam and diffuse solar radiation Radiation penetration through the water surface is largely a function of solar altitude and transmission through the water column is more of a function of water column depth Water column turbidity will also alter attenuation and scattering and thus the water transmission of radiation The stream bed will reflect a portion of received solar radiation as a function of received radiation solar altitude and substrate properties All radiant heat that is absorbed by the stream bed is treated separately in the stream bed conduction heat transfer pathway Radiation reflected from the stream bed is subjected to the same path length and transmission rates through the water column experienced from the surface to the stream bed Page 29 Chapter Il Heat Transfer Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 2 2 1 SOLAR TIME RELATIVE TO EARTH All expressions presented in this section are taken from Meeus 1988 and 1991 Definition of terminology taken largely from The Astronomical Almanac 1998 The Gregorian calendar time corrected for daylight savings refers to the calendar introduced by Pope Gregory XIII in 1582 to replace the Julian cal
251. you know that the area between the banks is stream channel This needs to become a single polygon within the riparian vegetation map and here is how to do tt 13 Under the XTools drop down menu select Make one polygon from polylines 14 Select the MERGED stream banks theme that you created in step 7 15 Name the new file this is also a temporary file that can eventually be deleted Page 168 Chapter V Spatial Data Derivations Analytical Methods for Dynamic Open Channel Heat and Mass Transfer Methodology for the Heat Source Model Version 7 0 Now you have your 300 foot riparian buffer polygon and a stream channel polygon Your next task is to combine these polygons See image below ArcView GIS Yersion 3 1 Eile Edit Yiew Theme Analysis Surface Graphics Tools Window Help CSD ESICUCTWIS FAR kobe Seer OO ERY A Plygont shp A Buffer 1 of Merge2 f Merge2 shp i _ Syean_right_ogic s Ane r e Riparian Buffer Ra Polygon _ Ttoob_data_ogic st 1 spar on Stream Channel Polygon mj Prai ogic shp Ej A ogic sl _ Trout Sj 301 sco F ioo 7s EE asi ject mn EF Bl Kamea 16 Turn on the extension called Geoprocessing 17 In the View menu select the Geoprocessing Wizard option 18 Select Union two themes 19 The input theme to union must be your stream channel polygon The polygon overlay theme to union must be yo

Heat Source Model User Guide - Department of Environmental Quality

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