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COMET University Faculty Hydrometeorology Course June 2000. Dennis L. Johnson. Dennis L. Johnson, Asst. Professor Juniata College Environmental Science & Studies (814) 641-5335 (Phone) (814) 641 – 3685 (Fax) Johnson@juniata.edu (Email) Http://www.Juniata.edu/~johnson/. Usual Houghton.

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Presentation Transcript
slide2

Dennis L. Johnson, Asst. ProfessorJuniata CollegeEnvironmental Science & Studies(814) 641-5335 (Phone)(814) 641 – 3685 (Fax)Johnson@juniata.edu (Email)Http://www.Juniata.edu/~johnson/

the runoff picture
The Runoff Picture
  • Hydrology is long term and short term….
  • In this course we will mainly focus on the short term:
  • Floods & flood flows.
  • Generating runoff/high flows.
  • Predicting/forecasting flows.
  • Space/time scales.
what s a flood
What’s a Flood?
  • What is a flood?????
  • A rather elusive definition
  • Generally contains terms like:
    • High water
    • High flows
    • Normal water course
    • Human impact(s)
    • Etc…
recipe s for a flood
Recipe(s) for a Flood
  • What causes a flood?
  • What are the conditions?
  • What are the types of flooding situations?
  • Your area or other areas…..
my recipes
My Recipes
  • “BIG” heavy soaking rains…
  • Low infiltration rates
  • Snow melt
  • Rain on snow
  • Very intense precipitation
  • Dam failure
  • Others….??
does a flood have to happen in a defined water course or waterway

Does a Flood Have to Happen in a Defined Water Course or Waterway?

….and If a Flood Does Occur in an Overland Situation – Does the Nearest Stream Even Feel It?

fema nfip www fema gov nfip
FEMA - NFIP…(www.fema.gov/nfip)

Flood--A general and temporary condition of partial or complete inundation of normally dry land areas from:

Overflow of inland or tidal waters.

The unusual and rapid accumulation or runoff of surface waters from any source.

Mudslides (i.e., mudflows) which are proximately caused by flood, as defined above, and are akin to a river of liquid and flowing mud on the surface of normally dry land areas, as when earth is carried by a current of water and deposited along the path of the current.

The collapse or subsidence of land along the shore of a lake or other body of water as a result of erosion or undermining caused by waves or currents of water exceeding the cyclical levels which result in flood, as defined above.

what are the defining characteristics of a flood
What Are the Defining Characteristics of a Flood?
  • Timing – rise time, recession, duration.
  • Flows – peak flows, magnitude (statistical).
  • Precipitation – intensity, duration, frequency….
what controls the timing flow and precipitation
What Controls the Timing, Flow, and Precipitation?
  • The hydrology – short term and long term.
  • The meteorology – short term (weather/storm type) and long term (climate).
big picture

Big Picture

Long term and short term

some of the right combinations
Some of the “Right” Combinations….
  • Precipitation –vs.- infiltration
    • Precipitation intensity > infiltration rate
    • Precipitation total > infiltration capacity
    • “Storage” in the system is full
    • Human induced high water or flows
    • Natural alterations to the watershed
our focus
Our Focus
  • More on the short term..
  • The combination(s) of precipitation and hydrologic conditions that lead up to a potential flooding situation…
  • “basin hydrology” – although basin hydrology looks at the long term hydrologic budget, as well.
let s take a minute to look at hydrology and the properties units concepts terminology

Let’s Take a Minute to Look at Hydrology and the Properties, Units, Concepts, & Terminology

hydrology

Hydrology

… An Earth Science. It Encompasses the Occurrence, Distribution, Movement, and Properties of the Waters of the Earth and Their Environmental Relationships." (Viessman, Knapp, Lewis, & Harbaugh, 1977 - Introduction to Hydrology, Harper & Row Publishers, New York)

slide20

History of Hydrology

(Hydrometeorology)

early on
Early on….
  • Early philosophers speculated on the hydrologic cycle:
  • Homer believed that there existed large subterranean reservoirs that fed the rivers, seas, springs, and wells - was he wrong?
  • Homer did understand the dependence of flow in the Greek aqueducts on conveyance and velocity!
history cont
History, Cont....
  • In the first century B.C., Marcus Vitruvius in the treatise de Architectura Libri Decem (the engineers chief handbook), vol. 8 hypothesized that rain and snow falling in the mountains infiltrated into the earth’s surface and appeared in the lowlands as springs and streams.....
early success
Early Success.....
  • 4000 b.C. The Egyptians built a dam on the Nile to allow barren lands to again be used for agricultural purposes.
more early successes
More Early Successes
  • 1000’s of years later, a canal to carry fresh water from Cairo to Suez was built.
  • Towns in Mesopotamia were protected by flooding from high earthen walls.
early disputes and rules
Early Disputes and Rules
  • The cities of Lagash and Umma of Mesopotamia have documented water disputes.
  • The Romans decree:
  • Ne quis aquam oletato dolo malo ubi publice saliet si quis oletarit sestertiorum X mila multa esto.
  • It is forbidden to pollute the public water supply; Any deliberate offender shall be punished by a fine of 10,000 sesterces!
qualitative understanding
Qualitative Understanding
  • Near end of 15th century, Leonardo da Vinci and Bernard Palissy independently reached conclusions on the hydrologic cycle - based on a philosophical understanding.
  • There was still a lack of quantitative understanding of the hydrologic cycle.
the 17th century
The 17th Century
  • Perrault, Mariotte, and Halley began quantitative measurements and applications.
  • Perrault measured rainfall and runoff over the seine river drainage basin for ~ 3 years - he illustrated that rainfall WAS adequate in quantity to account for river flows.
  • Mariotte gauged the velocity of the flow in the river seine and estimated flows by also estimating river cross sectional areas.
  • Halley was an astronomer! He estimated evaporation from the Mediterranean sea and correlated it to river flows into the med, concluding that river flows were sufficient enough to provide that volume of water.
the 18th century
The 18th Century
  • Bernoulli - famous for hydraulics and fluid mechanics - the piezometer, the pitot tube, and Bernoulli’s theorem.
  • The Chezy formula (channel flow).
the 19th century
The 19th Century
  • Hagen-Poiseuille - capillary flow equation.
  • Darcy’s - flow in porous media.
  • Duptuit-Thien well formula.
  • Manning - open channel flow.
  • Systematic stream gaging.
  • Mostly empirical in nature.
the 20th century
The 20th Century
  • Government agencies began to develop programs – good or bad?
  • Rational analysis begins.
  • Sherman - unit hydrograph theory.
  • Horton - infiltration theory.
  • Snyder - unit hydrograph.
  • Clark - unit hydrograph.
  • Etc...........
modern day
Modern Day
  • Very computer and data intensive
  • High tech instruments
  • Scale issues
  • Policy issues
  • Etc.................
  • “Diamond edge on an old axe”……
the watershed
The Watershed
  • A watershed is an area of land that drains to a single outlet and is separated from other watersheds by a divide.
  • Every watershed has a drainage area.
  • Related terms: drainage basin, sub-basin, sub-area.
slide34
Area
  • 1 acre = 43,560 ft2
  • 1 mi2 = 640 acres
  • 1 hectare = 100m x 100m = 2.471 acres = 10,000 m2
  • 1 km2 = 0.386 mi2
volume
Volume
  • 1 acre-foot = 1 ac-ft = 1 acre of water x 1 foot deep = 43,560 x 1 = 43,560 ft3.
  • 1 ac-inch = 1 acre x 1 inch deep = 43,560 x 1/12 = 3,630 ft3.
  • 1 ft3 = 7.48 gallons.
  • 1 gallon H2O ~ 8.34 lbs.
runoff volume
Runoff Volume
  • 1-inch of runoff over 1 square mile :
  • 1/12 feet x 1 mi2 x 640 acres/mi2 x 43,560 ft2/mi2 = 2,323,200 ft3
discharge
Discharge
  • 1 cfs = 1 cubic foot per second
  • 1 cfs x 7.48 gal/ft3 x 3600 sec/hr x 24 hrs/day = 646,272 gpd = 0.646 MGD
  • 1 cfs x 3600 sec/hr x 24 hrs/day = 86,400 cfs/day
  • 86,400 cfs/day x 1 ac-ft/43,560 ft3 = 1.983 ac-ft/day (~ 2 ac-ft/day)
  • 1.983 ac-ft/day x 12 inches/ft x 1 day/24 hrs = 0.992 ac-in/hr
  • 1 ac-in/hr x 43,560 ft3/ac-ft x 1 hr/3600 sec x 1 ft/12 inches = 1.008 cfs
power
Power
  • Hp = gHQ/550
  • 1 hp = 550 ft*lb/sec = 0.7547 kilowatts
hydrology terminology
Hydrology Terminology
  • Streamflowis the movement of water through a channel.
  • Thecross-sectional areaof a stream is the region bounded by the walls of the stream and the water surface. The cross-sectional area is illustrated below.
  • See alsoManning’s “n”.

Cross-sectional Area

Stream Flow

hydrology terminology40

Diagram 1

Diagram 2

Hydrology Terminology
  • Manning’s “n”is a measure of the roughness of a surface, and in streamflow it is the roughness of the channel bottom and it’s sides.

Diagram 2 will have a higher Manning’s “n” because it has rougher surface due to the jagged bottom and pebbles.

hydrology terminology41

Routing

Hydrologic

Hydraulic

Hydrology Terminology
  • Routing is used to account for storage and translation effects.
hydrology terminology42
Hydrology Terminology

Generalized effect of routing

hydrology terminology43
Hydrology Terminology
  • Snowfallis a form of precipitation that comes down in white or translucent ice crystals.
  • Snowmeltis the excess water produced by the melting of snow. This leads to flooding possibilities in the spring when temperatures begin to rise. There is generally a delay in the snowmelt response of a basin due to the melting process and travel times.
  • Snowpackis the amount of annual accumulation at higher elevations.
hydrology terminology44
Hydrology Terminology
  • Runoffis the excess precipitation and is often considered a “fast” response.
  • Overland flowis the flow of water across the land surface.
  • Sub-surface flowis the flow of water through the soil layers to the stream.
  • Baseflowis the flow in a channel due to ground water or subsurface supplies. The baseflow is generally increased by precipitation events that produce enough infiltration.
hydrology terminology45
Hydrology Terminology
  • Infiltrationis the movement of water from the surface into the soil.
  • The rate of infiltration is based on a number of factors, including but not limited to:
    • soil types
    • current conditions
    • precipitation intensity
hydrology terminology46
Hydrology Terminology
  • The velocity of the flow is very dependent on the slope of the stream bottom. The greater the slope the greater the potential velocity of the flow.
  • The “wave” speed is the velocity of the flood wave down the channel. The speed of this wave affects how quickly the downstream area will effected.
hydrology terminology47

Energy Grade Line

headloss

Hydraulic Grade Line

(water surface)

Depth1

Channel Bottom

Elevation Head

Depth2

Datum

Hydrology Terminology
  • Theenergy grade linerepresents the depth of the water surface and the velocity component of the Bernoulli equation.
  • Thehydraulic grade linerepresents the depth of the water surface.
hydrology terminology48
Hydrology Terminology
  • Karst hydrology is caused by pores and holes in limestone formations. This increases the infiltration into the limestone, reducing the runoff potential.
  • The slope changes the speed of runoff and therefore effects collection times.
hydrology terminology49
Hydrology Terminology
  • The frequency of a storm event is described by its return period. For example a two year storm event has a 1 in 2 chance of occurring in any given year.
  • The probability is also affected by the return period. Thus the probability of a 2 year storm occurring is 50%. The probability of a 100-year event occurring is 1/100 or 1%
precipitation
Precipitation
  • ... primary "input" for the hydrologic cycle (or hydrologic budget).
  • … The patterns of the precipitation are affected by large scale global patterns, mesoscale patterns, "regional" patterns, and micro-climates.
  • … In addition to the quantity of precipitation, the spatial and temporal distributions of the precipitation have considerable effects on the hydrologic response.
slide52
Snow
  • … response mechanisms of snow are at a much slower time scale than for most of the other forms of precipitation.
  • … The melt takes place and the runoff is "lagged" due to the physical travel processes.
  • … Items to consider in the snowmelt process are the current "state" of the pack and the snow water equivalent of the snow pack., as well as the melt potential of the current climate conditions.
  • … A rain-on-snow event may produce very high runoff rates and is often a difficult situation to predict due to the integral nature of the runoff and melt processes. The timing of these events is often very difficult to predict due to the inherent "lag" in the responses.
snow hydrology

Snow Hydrology

Special Thanks, Credit, and Recognition to Don Cline

And the

National Operational Hydrologic Remote Sensing Center

why is snow important55
Why is Snow Important?
  • Water Resources
  • Flooding
  • Economics
  • Transportation
snow hydrology56
Snow Hydrology
  • Understanding and predicting the physical processes of:
      • Snow Accumulation
      • Ablation
      • Melt Water Runoff
snow hydrology57
Snow Hydrology
  • 4 Simultaneous Estimation Problems
    • the quantity of water held in snow packs
    • the magnitude and rate of water lost to the atmosphere by sublimation
    • the timing, rate, and magnitude of snow melt
    • the fate of melt water
snow cover distribution59
Snow Cover Distribution
  • Three Spatial Scales
    • Macroscale
      • Areas up to 106 km2
      • Characteristic Distances of 10-1000 km
      • Dynamic meteorologic effects are important
    • Mesoscale
      • Characteristic Distances of 100 m to 10 km
      • Redistribution of snow along relief features due to wind
      • Deposition and accumulation of snow may be related to terrain variables and to vegetation cover
    • Microscale
      • Characteristic Distances of 10 to 100 m
      • Differences in accumulation result from variations in air flow patterns and transport
snow cover distribution60
Snow Cover Distribution
  • Effect of Topography
    • The depth of seasonal snow cover usually increases with elevation if other influencing factors do not vary with elevation
      • This trend is generally due to:
        • increase in the number of snowfall events
        • decrease in evaporation and melt
      • The rate of increase with elevation may vary widely from year-to-year
    • However, elevation alone is not a causative factor in snow cover distribution
      • Many other factors must be considered:
        • slope, aspect, vegetation, wind, temperature, and characteristics of the parent weather systems
snow cover distribution61
Snow Cover Distribution
  • Effect of Vegetation
    • Snow falling into a vegetation canopy is influenced by two phenomena:
      • Turbulent air flow above and within the canopy
        • may lead to variable snow input rates and microscale variation in snow loading on the ground
      • Direct interception of snow by the canopy elements
        • may either sublimate or fall to the ground
    • Processes are related to vegetation type, vegetation density, and the presence of nearby open areas
snow cover distribution62
Snow Cover Distribution
  • Forested Environments
    • Differences in snow accumulation between different species of conifers is usually small compared to between coniferous and deciduous stands
      • coniferous stands are all relatively efficient snow interceptors
      • Once intercepted, cohesion between snow particles helps keep snow in the canopy for extended time periods
        • snow is more susceptible to sublimation losses in the canopy than on the forest floor
          • High surface area to mass ratio
snow cover distribution63
Snow Cover Distribution
  • Forested Environments
    • Most studies show greater snow accumulation in clearings than in the forest
    • Most of the difference develops during storms, not between storms
      • redistribution of intercepted snow by wind to clearings is not typically a significant factor
    • Interception and subsequent sublimation are the major factors contributing to the difference

20-45%

Greater Snow

Accumulation

snow cover distribution64
Snow Cover Distribution
  • Open Environments
    • Over highly exposed terrain, the effects of meso- and micro-scale differences in vegetation and terrain features may produce wide variations in accumulation patterns.
snow cover distribution65
Snow Cover Distribution
  • Open Environments
    • Relative accumulation on various landscapes in an open grassland environment
      • Normalized to snow accumulation on level plains under fallow
blowing snow
Blowing Snow
  • Sublimation Losses
    • Snow particles are more exposed to atmosphere during wind transport
    • Sublimation losses can be very high as a result
      • depends on transport rate, transport distance, temperature, humidity, wind speed, and solar radiation
blowing snow67
Blowing Snow
  • Sublimation Losses

Mean Annual Blowing Snow Sublimation

CANADA, 1970-1976

Loss in mm SWE over 1 km

22

25

16

30

50

20

22

25

snow pack characteristics69
Snow Pack Characteristics
  • What is a Snow Pack?
    • Porous Medium
      • ice + air (+ liquid water)
    • Generally composed of layers of different types of snow
      • more or less homogeneous within one layer
    • Ice is in form of crystals and grains that are usually bonded together
      • forms a texture with some degree of strength
snow pack characteristics70
Snow Pack Characteristics
  • Snow Water Equivalent (SWE)
    • The height of water if a snow cover is completely melted, on a corresponding horizontal surface area.
      • Snow Depth x (Snow Density/Water Density)
density of snow cover
Density of Snow Cover

Snow Depth for

One Inch Water

Snow Type

Density (kg/m3)

Wild Snow

10 to 30

98” to 33”

Ordinary new snow immediately

after falling in still air

50 to 65

20” to 15”

Settling Snow

70 to 90

14” to 11”

Average wind-toughened snow

280

3.5”

350

2.8”

Hard wind slab

New firn snow

400 to 550

2.5” to 1.8”

Advanced firn snow

550 to 650

1.8” to 1.5”

Thawing firn snow

600 to 700

1.6” to 1.4”

snow pack characteristics72
Snow Pack Characteristics
  • Liquid Water Content
    • Wetness, Percentage by volume

Term

Remarks

Approximate Range

Usually T < 0oC, but can occur at any temperature up to 0oC. Little tendency for snow grains to stick together.

Dry

0%

T = 0oC. The water is not visible even at 10x magnification. Has a distinct tendency to stick together.

Moist

<3%

T = 0oC. The water can be seen at 10x magnification by its miniscus between grains, but cannot be pressed out by squeezing snow (pendular regime).

Wet

3-8%

T = 0oC. The water can be pressed out by squeezing snow, but there is an appreciable amount of air (funicular regime).

Very Wet

8-15%

T = 0oC. The snow is flooded with water and contains a relatively small amount of air.

Slush

>15%

snow characteristics
Snow Characteristics
  • Diurnal Temperature Gradients
water flow through snow75
Water Flow through Snow
  • Wide Range of Flow Velocities
    • 2 - 60 cm/min
    • Depends on several factors
      • internal snow pack structure
      • condition of the snow pack prior to introduction of water
      • amount of water available at the snow surface
water flow through snow76
Water Flow Through Snow
  • Flow through Homogeneous Snow
    • At melting temperature, a thin film of water surrounds each snow grain
      • Much of the water can flow through this film
    • Once pores are filled, laminar flow can occur
      • Very efficient mechanism for draining the snow pack
water flow through snow77
Water Flow through Snow
  • Four Liquid Water Regimes
      • Capillary: < 1% free water
        • water doesn’t drain due to capillary tension
      • Unsaturated: 1-14% free water
        • water drains by gravity, but air spaces are continuous
        • Pendular Regime
      • Saturated: > 14% free water
        • water drains by gravity, but air spaces are discontinuous
        • Funicular Regime
      • Melt/Freeze
        • water melts and refreezes, possible several times, before it drains from the snow pack
water flow through snow78
Water Flow Through Snow
  • Flow through Heterogeneous Snow
    • Preferential Flow Paths
      • Dye studies reveal vertical channels or macropores in most natural snowpacks
    • Ice Layers
      • Develop from surface melt or refreezing
      • Relatively impermeable
      • Forces ponding of water and lateral flow

Ice Lens

with Ponding

Preferential Flow Paths

Water Flow

Ice Lens

water flow through snow79
Water Flow Through Snow
  • Liquid Water Transmission

Melt and rain water are

lagged and attenuated as they move through the snow cover.

Function of depth, density, ice layers, grain size, and refreezing.

Rain

snow measurement81
Snow Measurement
  • Snow Water Equivalent (SWE)
    • Ground Observations
      • Snow Pillows
        • SNOTEL Sites (Western U.S.)
      • Snow Courses
        • Transects with snow depth and density
      • Snow Tubes
        • measure volume and mass of snow cores
      • Snow Pits
        • Measure vertical profiles of SWE, and other snow pack variables.
snow measurement82
Snow Measurement
  • Airborne Snow Survey Program (SWE)
snow measurement83
Snow Measurement
  • Satellite Areal Extent of Snow Cover
snow measurement84
Snow Measurement
  • NOAA-16 1.6 Micron Channel
snow measurement85
Snow Measurement
  • NOAA-16 1.6 Micron Channel

Snake River Valley, Idaho

SNOW

Visible Channel

1.6 micron Channel

evaporation
Evaporation
  • … Evaporation is a process that allows water to change from its liquid phase to a vapor.
  • … Hydrologists are mostly interested in the evaporation from the free water surface of open water or subsurface water exposed via the capillary action; however, precipitation that is intercepted by the vegetative canopy may also be evaporated and may be a significant amount in terms of the overall hydrologic budget.
  • … Factors that affect evaporation are temperature, humidity and vapor pressure, radiation, and wind speed.
  • … A number of equations are used to estimate evaporation. There are also a number of published tables and maps providing regional estimates of annual evaporation.
transpiration
Transpiration
  • … Water may also pass to the atmosphere by being "taken up" by plants and passed on through the plant surfaces.
  • … Transpiration varies greatly between plants or crops, climates, and seasons.
  • … Evaporation and transpiration are often combined in a term - evapotranspiration.
  • … In many areas of the country and during certain seasons evapotranspiration is a major component of the hydrologic budget and a major concern in water supply and yield estimates.
storage surface
Storage - Surface
  • ... Storage - Surface is used to describe the precipitation that reaches the ground surface; however, is not available for runoff or infiltration.
  • … It is instead, held in small quantities on the surface in areas, such as the leafy matter and small depressions.
  • … In general, surface storage is small and only temporary in terms of the overall hydrologic budget; however, it may have an effect on a storm response as it is effectively "filled" early on a storm event.
infiltration
Infiltration
  • … Soils, depending on current conditions, have a capacity or ability to infiltrate precipitation, allowing water to move from the surface to the subsurface.
  • ... "physically based” -> soil porosity, depth of soil column, saturation levels, and soil moisture.
  • … The infiltration capacity of the soil column is usually expressed in terms of length per time (i.e. inches per hour).
  • … As more water infiltrates, the infiltration generally decreases, thus the amount of water that can be infiltrated during the latter stages of a precipitation event is less than that at the beginning of the event.
infiltration cont

Infiltration cont.

… Storms that have high intensity levels may also cause excess precipitation because the intensity (inches per hour) may exceed the current infiltration capacity (inches per hour).

… periods of low rainfall or no rainfall will allow the soil to "recover" and increase the capacity to infiltrate water.…

Infiltrated water replenishes soil moisture and groundwater reservoirs. Infiltrated water may also resurface to become surface flow.

… attempt to account for infiltration by estimating excess precipitation (the difference between precipitation and excess being considered infiltration), for example, the Soil Conservation Service (SCS) runoff curve number method

subsurface flow

Subsurface Flow

…water may move via several paths.

…subsurface flow can be evaporated if there is a well maintained transfer mechanism to the surface. This is particularly true for areas of high ground water table (the free water surface of the groundwater) which is within the limits of the capillary action or transport abilities.

…Vegetation may also transpire or use the water.

…The subsurface flow may also continue to move with the groundwater table as a subsurface reservoir, which the natural system uses during periods of low precipitation.

storage subsurface
Storage - Subsurface
  • … The infiltrated water may continue downward in the vertical, may move through subsurface layers in a horizontal fashion, or a combination of the two directions.
  • … Movement through the subsurface system is much slower than the surface and thus there are storage delays. The water may also reach an aquifer, where it may be stored for a very long period of time.
runoff
Runoff
  • … runoff will be used to collectively describe the precipitation that is not directly infiltrated into the groundwater system.
  • … is generally characterized by overland, gully and rill, swale, and channel flows.
  • … is that portion of a precipitation event that "quickly" reaches the stream system. The term "quickly" is used with caution as there may be great variability in response times for various flow mechanisms.
  • … Runoff producing events are usually thought of as those that saturate the soil column or occur during a period when the soil is already saturated. Thus infiltration is halted or limited and excess precipitation occurs. This may also occur when the intensity rate of the precipitation is greater than the infiltration capacity.
overland flow

Overland Flow

… Overland flow or surface flow is that precipitation that either fails to penetrate into the soil or that resurfaces at a later point due to subsurface conditions.

… often referred to as "sheet" flow.

… for the purposes of this discussion, overland flow (sheet and surface flow, as well) is considered to be the flow that has not had a chance to collect and begin to form gullies, rills, swales

overland flow cont

Overland Flow (cont.)

… will eventually reach defined channels and the stream system.

… may also be infiltrated if it reaches an area that has the infiltration capacity to do so.

… Overland flow distances are rather limited in length - National Engineering Handbook (1972) - overland flow will concentrate into gullies in less than 1000 feet.

… Other (Seybert, Kibler, and White 1993) recommend a distance of 100 feet or less.

gullies rills

Gullies & Rills

... sheet flow or overland flow will soon concentrate into gullies and rills in the process of flowing towards the stream network. The location of these gullies and rills may vary from storm to storm, depending on storm patterns, intensities, current soil and land use conditions.

swales

Swales

… swales are of a more constant or permanent nature.

… do not vary in location from storm to storm.

… Swales are a natural part of the landscape or topography that are often more apparent than gullies and rills.

… Flow conditions and behaviors in swales are very close to that which is seen in channels.

channel flow

Channel Flow

… Excess precipitation ultimately reaches the stream channel system.

… the stream system is generally more defined, it is by no means a constant or permanent entity.

… The stream bed is constantly changing and evolving via aggredation and degradation.

… Stream channels convey the waters of the basin to the outlet and into the next basin.

… attenuation of the runoff hydrograph takes place.

… Stream channel properties (flow properties) also vary with the magnitude of the flow.

stream channels

Stream Channels

… Channels are commonly broken into main channel areas and overbank areas.

… overbank areas are often referred to as floodplains.

… Stream gaging stations are used to determine flows based on elevations in the channel and/or floodplain.

… Bank full is often thought of as flood stage although more rigorous definitions are more applicable as they pertain to human activity and potential loss of life and property.

… It is worth noting that the 2-year return interval flow is often thought of as "bank-full".

streamflow
Streamflow
  • … in the public eye -> the most important aspect of flooding and hydrology.
  • … flooding from streams and rivers have the greatest potential to impact human property and lives; although overland flow flooding, mudslides, and landslides are often just as devastating.
  • … Subsurface flow also enters the stream; although in some instances and regions, stream channels lose water to the groundwater table - regardless, this must be accounted for in the modeling of the stream channel.
  • … Channels also offer a storage mechanism and the resulting effect is most often an attenuation of the flood hydrograph.
storage reservoirs
Storage - Reservoirs
  • … Lakes, reservoirs, & structures, etc. are given a separate category in the discussion of the hydrologic cycle due to the potential impact on forecasting procedures and outcomes.
  • … provide a substantial storage mechanism and depending on the intended purpose of the structure will have varying impacts on the final hydrograph, as well as flooding levels.
  • … This effect can vary greatly depending on the type of reservoir, the outlet configuration, and the purpose of the reservoir.
storage reservoirs cont
Storage - Reservoirs (cont.)
  • … Flood control dams are used to attenuate and store potentially destructive runoff events.
  • … Other structures may have adverse effects. For example, bridges may cause additional "backwater" effects and enhance the level of flooding upstream of the bridge.
  • … a catastrophic failure of a structure often has devastating effects on loss of life and property.
simulating the hydrologic response
Simulating the Hydrologic Response

Model Types

Precipitation

Losses

Modeling Losses

Model Components

model types
Model Types

Model Types

Precipitation

Losses

Modeling Losses

Model Components

  • Empirical
  • Analytical
  • Lumped
  • Distributed
general goal of most models
General Goal of Most Models

Infiltration

Excess Precip.

Interception

Storage

Basin Process Representation

Time Series

Time Series

We must begin to think of the basin as a “whole”

the basic process
The Basic Process

Excess Precip. Model

Excess Precip.

Runoff Hydrograph

Basin “Routing”

Excess Precip.

Downstream Hydrograph

Stream “Routing”

Runoff Hydrograph

from a basin view
From A Basin View

Excess Precip.

Excess Precip. Model

Basin “Routing”

Runoff Hydrograph

Stream “Routing”

precipitation input
Precipitation Input
  • Precipitation is generally “pre-processed
  • Uniform in space and time – never!
  • Gages
  • Radar
  • satellite
precipitation109
Precipitation
  • … magnitude, intensity, location, patterns, and future estimates of the precipitation.
  • … In lumped models, the precipitation is input in the form of average values over the basin. These average values are often referred to as mean aerial precipitation (MAP) values.
  • … MAP's are estimated either from 1) precipitation gage data or 2) NEXRAD precipitation fields.
precipitation cont
Precipitation (cont.)
  • … If precipitation gage data is used, then the MAP's are usually calculated by a weighting scheme.
  • … a gage (or set of gages) has influence over an area and the amount of rain having been recorded at a particular gage (or set of gages) is assigned to an area.
  • … Thiessen method and the isohyetal method are two of the more popular methods.
thiessen
Thiessen
  • Thiessen methodis a method for areally weighting rainfall through graphical means.
isohyetal
Isohyetal
  • Isohyetal methodis a method for areally weighting rainfall using contours of equal rainfall (isohyets).
nexrad
NEXRAD
  • Nexradis a method of areally weighting rainfall using satellite imaging of the intensity of the rain during a storm.
excess precip models
Excess Precip. Models
  • Physically Based
  • Empirical
  • Analytical
  • Conceptual
  • Generally Lumped
losses
Losses
  • … modeled in order to account for the destiny of the precipitation that falls and the potential of the precipitation to affect the hydrograph.
  • … losses include interception, evapotranspiration, depression storage, and infiltration.
  • … Interception is that precipitation that is caught by the vegetative canopy and does not reach the ground for eventual infiltration or runoff.
  • … Evapotranspiration is a combination of evaporation and transpiration and was previously discussed.
  • … Depression storage is that precipitation that reaches the ground, yet, as the name suggests, is stored in small surface depressions and is generally satisfied during the early portion of a storm event.
modeling losses
Modeling Losses
  • … simplistic methods such as a constant loss method may be used.
  • … A constant loss approach assumes that the soil can constantly infiltrate the same amount of precipitation throughout the storm event. The obvious weaknesses are the neglecting of spatial variability, temporal variability, and recovery potential.
  • Other methods include exponential decays (the infiltration rate decays exponentially), empirical methods, and physically based methods.
  • … There are also combinations of these methods. For example, empirical coefficients may be combined with a more physically based equation. (SAC-SMA for example)
estimating s
Estimating “S”
  • The difficult part of applying this method to a watershed is the estimation of the watershed’s potential maximum retention, S.
  • SCS developed the concept of the dimensionless curve number, CN, to aid in the estimation of S.
  • CN is related to S as follows :

CN ranges from 1 to 100 (not really!)

determine cn
Determine CN
  • The Soil Conservation Service has classified over 8,500 soil series into four hydrologic groups according to their infiltration characteristics, and the proper group is determined for the soil series found.
  • The hydrologic groups have been designated as A, B, C, and D.
  • Group A is composed of soils considered to have a low runoff potential. These soils have a high infiltration rate even when thoroughly wetted.
  • Group B soils have a moderate infiltration rate when thoroughly wetted,
  • while group C soils are those which have slow infiltration rates when thoroughly wetted.
  • Group D soils are those which are considered to have a high potential for runoff, since they have very slow infiltration rates when thoroughly wetted (SCS, 1972).
determine cn cont
Determine CN, cont….
  • Once the hydrologic soil group has been determined, the curve number of the site is determined by cross-referencing land use and hydrologic condition to the soil group - SAMPLE

Land use and treatment Hydrologic soil group

or Hydrologic

practice condition A B C D

Fallow

Straight row ---- 77 86 91 94

Row Crops

Straight row Poor 72 81 88 91

Straight row Good 67 78 85 89

Contoured Poor 70 79 84 88

initial conditions
Initial Conditions

5-day antecedent rainfall, inches

Antecedent moisture

Dormant Season Growing Season

I Less than 0.5 Less than 1.4

II 0.5 to 1.1 1.4 to 2.1

III Over 1.1 Over 2.1

sac sma

Upper Zone

Tension

Free

Lower Zone

Tension

Free - Primary

Free - Supplemental

SAC-SMA
  • … The Sacramento Soil Moisture Accounting Model (SAC-SMA) is a conceptual model of soil moisture accounting that uses empiricism and lumped coefficients to attempt to mimic the physical constraints of water movement in a natural system.
runoff125
Runoff
  • … Runoff is essentially the excess precipitation - the precipitation minus the losses.
  • … Runoff must be transformed to streamflow at the basin outlet via a unit hydrograph.
  • … In actuality, all forms of surface and subsurface flow that reach a stream channel and eventually the outlet are modeled through the use of the unit hydrograph for the general hydrologic model…
unit hydrograph theory
Unit Hydrograph Theory
  • Sherman - 1932
  • Horton - 1933
  • Wisler & Brater - 1949 - “the hydrograph of surface runoff resulting from a relatively short, intense rain, called a unit storm”
  • The runoff hydrograph may be “made up” of runoff that is generated as flow through the soil (black, 1990)
linearity of unit hydrograph
Linearity of Unit Hydrograph
  • … In addition, when unit hydrograph theory is applied, it is assumed that the watershed responds uniformly.
  • … Meaning that peak flow from 2 inches of excess will be twice that of 1 inch of excess
unit hydrograph lingo
Unit Hydrograph “Lingo”
  • Duration
  • Lag Time
  • Time of Concentration
  • Rising Limb
  • Recession Limb (falling limb)
  • Peak Flow
  • Time to Peak (rise time)
  • Recession Curve
  • Separation
  • Base flow
graphical representation
Graphical Representation

Duration of excess precipitation.

Lagtime

Timeofconcentration

Baseflow

methods of developing uhg s
Methods of Developing UHG’s
  • From Streamflow Data
  • Synthetically
    • Snyder
    • SCS
    • Time-Area (Clark, 1945)
  • “Fitted” Distributions
unit hydrograph
Unit Hydrograph
  • The hydrograph that results from 1-inch of excess precipitation (or runoff) spread uniformly in space and time over a watershed for a given duration.
  • The key points :
      • 1-inch of EXCESS precipitation
      • Spread uniformly over space - evenly over the watershed
      • Uniformly in time - the excess rate is constant over the time interval
      • There is a given duration
derived unit hydrograph134
Derived Unit Hydrograph
  • Rules of Thumb :
  • … the storm should be fairly uniform in nature and the excess precipitation should be equally as uniform throughout the basin. This may require the initial conditions throughout the basin to be spatially similar.
  • … Second, the storm should be relatively constant in time, meaning that there should be no breaks or periods of no precipitation.
  • … Finally, the storm should produce at least an inch of excess precipitation (the area under the hydrograph after correcting for baseflow).
separation of baseflow
Separation of Baseflow
  • ... generally accepted that the inflection point on the recession limb of a hydrograph is the result of a change in the controlling physical processes of the excess precipitation flowing to the basin outlet.
  • In this example, baseflow is considered to be a straight line connecting that point at which the hydrograph begins to rise rapidly and the inflection point on the recession side of the hydrograph.
  • the inflection point may be found by plotting the hydrograph in semi-log fashion with flow being plotted on the log scale and noting the time at which the recession side fits a straight line.
sample calculations
Sample Calculations
  • In the present example (hourly time step), the flows are summed and then multiplied by 3600 seconds to determine the volume of runoff in cubic feet. If desired, this value may then be converted to acre-feet by dividing by 43,560 square feet per acre.
  • The depth of direct runoff in feet is found by dividing the total volume of excess precipitation (now in acre-feet) by the watershed area (450 mi2 converted to 288,000 acres).
  • In this example, the volume of excess precipitation or direct runoff for storm #1 was determined to be 39,692 acre-feet.
  • The depth of direct runoff is found to be 0.1378 feet after dividing by the watershed area of 288,000 acres.
  • Finally, the depth of direct runoff in inches is 0.1378 x 12 = 1.65 inches.
obtain uhg ordinates
Obtain UHG Ordinates
  • The ordinates of the unit hydrograph are obtained by dividing each flow in the direct runoff hydrograph by the depth of excess precipitation.
  • In this example, the units of the unit hydrograph would be cfs/inch (of excess precipitation).
determine duration of uhg
Determine Duration of UHG
  • The duration of the derived unit hydrograph is found by examining the precipitation for the event and determining that precipitation which is in excess.
  • This is generally accomplished by plotting the precipitation in hyetograph form and drawing a horizontal line such that the precipitation above this line is equal to the depth of excess precipitation as previously determined.
  • This horizontal line is generally referred to as the F-index and is based on the assumption of a constant or uniform infiltration rate.
  • The uniform infiltration necessary to cause 1.65 inches of excess precipitation was determined to be approximately 0.2 inches per hour.
estimating excess precip
Estimating Excess Precip.

0.8

0.7

0.6

0.5

Uniform loss rate of

0.2 inches per hour.

Precipitation (inches)

0.4

0.3

0.2

0.1

0

0

1

2

3

4

5

6

7

8

9

10

11

12

13

14

15

16

17

18

19

Time (hrs.)

average several uhg s
Average Several UHG’s
  • It is recommend that several unit hydrographs be derived and averaged.
  • The unit hydrographs must be of the same duration in order to be properly averaged.
  • It is often not sufficient to simply average the ordinates of the unit hydrographs in order to obtain the final unit hydrograph. A numerical average of several unit hydrographs which are different “shapes” may result in an “unrepresentative” unit hydrograph.
  • It is often recommended to plot the unit hydrographs that are to be averaged. Then an average or representative unit hydrograph should be sketched or fitted to the plotted unit hydrographs.
  • Finally, the average unit hydrograph must have a volume of 1 inch of runoff for the basin.
one step shy of a full derivation
One Step Shy of a Full Derivation?
  • You could part of the previous analysis for a very useful tool.
  • Take a storm
  • Plot streamflow
  • Determine volume of runoff
  • Divide by basin area
  • Get depth of runoff
  • Estimate total basin (mean) precipiation
  • Compare!
  • Do this for a variety of storm over a variety of conditions and seasons.
synthetic uhg s
Synthetic UHG’s
  • Snyder
  • SCS
  • Time-area
snyder
Snyder
  • Since peak flow and time of peak flow are two of the most important parameters characterizing a unit hydrograph, the Snyder method employs factors defining these parameters, which are then used in the synthesis of the unit graph (Snyder, 1938).
  • The parameters are Cp, the peak flow factor, and Ct, the lag factor.
  • The basic assumption in this method is that basins which have similar physiographic characteristics are located in the same area will have similar values of Ct and Cp.
  • Therefore, for ungaged basins, it is preferred that the basin be near or similar to gaged basins for which these coefficients can be determined.
final shape

Final Shape

The final shape of the Snyder unit hydrograph is controlled by the equations for width at 50% and 75% of the peak of the UHG:

triangular representation156
Triangular Representation

The 645.33 is the conversion used for delivering 1-inch of runoff (the area under the unit hydrograph) from 1-square mile in 1-hour (3600 seconds).

slide157
484 ?

Comes from the initial assumption that 3/8 of the volume under the UHG is under the rising limb and the remaining 5/8 is under the recession limb.

time of concentration
Time of Concentration
  • Regression Eqs.
  • Segmental Approach
a regression equation
A Regression Equation

where : Tlag = lag time in hours

L = Length of the longest drainage path in feet

S = (1000/CN) - 10 (CN=curve number)

%Slope = The average watershed slope in %

segmental approach
Segmental Approach
  • More “hydraulic” in nature
  • The parameter being estimated is essentially the time of concentration or longest travel time within the basin.
  • In general, the longest travel time corresponds to the longest drainage path
  • The flow path is broken into segments with the flow in each segment being represented by some type of flow regime.
  • The most common flow representations are overland, sheet, rill and gully, and channel flow.
a basic approach
A Basic Approach

McCuen (1989) and SCS (1972) provide values of k for several flow situations (slope in %)

Sorell & Hamilton, 1991

hypothetical example
Hypothetical Example
  • A 190 mi2 watershed is divided into 8 isochrones of travel time.
  • The linear reservoir routing coefficient, R, estimated as 5.5 hours.
  • A time interval of 2.0 hours will be used for the computations.
rule of thumb
Rule of Thumb

R - The linear reservoir routing coefficient can be estimated as approximately 0.75 times the time of concentration.

trouble getting a time area curve
Trouble Getting a Time-Area Curve?

Synthetic time-area curve - The U.S. Army Corps of Engineers (HEC 1990)

instantaneous uhg
Instantaneous UHG
  • Dt = the time step used n the calculation of the translation unit hydrograph
  • The final unit hydrograph may be found by averaging 2 instantaneous unit hydrographs that are a Dt time step apart.
let s talk about modeling issues

Let’s talk about Modeling Issues

Weaknesses, strengths, etc…

factors affecting the hydrologic response
Factors Affecting the Hydrologic Response
  • Current Conditions
  • Precipitation Patterns
  • Land Use
  • Channel Changes
  • Others…..
channel changes
Channel Changes
  • Slopes
  • Storage
  • Rating Curve
variable source area concept

Variable Source Area Concept

Not all of the watershed is contributing during an event......

small basin hydrology

Small Basin Hydrology

and

Distributed Models

causes of non homogeneity
Causes of Non-homogeneity
  • Small scale precipitation
  • Spatially diverse precipitation patterns
  • Small scale basin changes – i.e. soil moisture, slope, etc….
  • Sub-basin changes – urbanization
  • Others????
hydrology terminology187
Hydrology Terminology
  • Precipitation can fall in many different patterns, which influences the hydrologic response.
  • For example, a storm may be:
    • Uniform over the entire watershed
    • A storm may move up the watershed
    • A storm may move down the watershed
    • A storm may only rain on a portion of the watershed.
approaches
Approaches
  • Many sub-basins – at least more than you currently have…
  • Hillslope processes
  • TIN’s
  • Grids - raster
common with lumped
Common with Lumped
  • Still must compute excess
  • Can still use empirical, analytical, conceptual, etc….
computationally
Computationally
  • Huge demands computationally
  • Must now keep track of flow, precip, moisture, etc.. On hundreds to thousands of pixels, sub-basins, etc….
moving water off basin
Moving water off basin
  • Lumped we tended to use the UHG
  • Now we tend to be more physically based:
    • Hydraulic equation
    • Hydrologic routing
    • Etc….