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midterm Flashcards

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1
Q

hydrolic system

A

structure/volume in space surronded by boundary, acceping water or other inputes and produces output

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2
Q

hydrosphere

A

where water on earth is in atomphsers and litosphere

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3
Q

water cycle

A

how water ciruclates through hydrosphere, no beginining or end and conitnuous

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4
Q

Key parts water cycle

A

evaporation: water turns to vapour goes up
Evapotrasnpiration: Water evaporation + transpiration from plants
Sublimation: From solid to gas instnatly
COndensation: From vapor to water in sky
Precipitation: Falling moisture to groud
Infiltartion: Enter ground
Runoff: Excess water

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5
Q

Watershed:

A

land that drains to lowest hydrographic feature. Sperated by surface/watershed divide. One watershed can be divided to subsystems

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6
Q

watershed types

A

closed: flow in boundaries
open: flow exits through outlet

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7
Q

Watershed characteristics

A

area
slope: more steep = more peek
shape more round = more peak
soil type more permeable = less runoff
land use urban vs nature vs forest

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8
Q

types of models

A

physical: representation of real world bud reduced: Used to simulate complex/difficult

math: approximate behavior of real world: Cheaper, asses many, large spatial scale

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9
Q

math model ttypes

A

lumped:: system = averaged and treat as point
distributed: various points in space
steady vs undstead: steady = same w/ time
event vs continuous: event is single, conitnunou = mutiple
deterministics vs stochastic: deterministic = same input to same output but stochastic = same input, diff output

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10
Q

Percipitation formation

A

lifting air mass into atmosphere to cool and condense
Mass lifting mechanisims:
Frontal: warm air and cold air come from opposite directions, warm air rises
Orogrpahic: air rises over mountain range, cause dry/wet spells
Convective: rises due to surfcae heatingL warm air causes air to go up from sun, why tropics are wet

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11
Q

Percipitation COnditions

A
  1. atmosphere = saturated(moist from ground)
  2. nuclei present for condenstaion/sublimation to occur
  3. Particles grow in size and can reach earth against winds(particles increase and decrease in size by condensation evaporation until big enough)
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12
Q

Percipitation classiification:

A

Drizzle: diamtere<0.5mm, intensity <1mm/hr
rain: d >0.5mm,
sleet: frozen raindrops due to cold air column
snow: ice crystal by sublimation
hail: ice particles due to upward wind cuasing increase in size

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13
Q

Variability in rain

A
  1. main is orthographic
  2. Heating uneven
    Equator = most surface radiation, poles = much less
    hadley cell, ferrel cell, polar cell create change in warm and cool air causing rain in areas
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14
Q

cells in heating

A

hadly = 0-30
ferrel = 30-50
polar = 50-90

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15
Q

temporal percipitation

A

changes with season due to teilt, changes movement in different seasons

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16
Q

Precipitation measurement

A

non-recording guage: collect rainwater over period of time but not record timing
recording gauge:
1. tipping bucket tipping back and forth, tips one into another reocrding time/amounts
2. Weighing gage: bucket is blaance and weight over time is recorded
3. Disdromoter optical device measure size/fall velocity by light beam w/ receiver reflecting off particles used to classify percipitation

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17
Q

Percipiation measure error

A
  1. wind
  2. evaporation loss
  3. calibration
  4. human
  5. feild issues
  6. positioning
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18
Q

Area measure sensor types

A
  1. microwave by reflect off particle
  2. infared detect temp of clouds
  3. visible: observe cloud cover, types ect.
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19
Q

Percipitation data

A
  1. Intensity, = depth/time, = volume/(area*time)
  2. hyetograph: historgram of epth/time
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20
Q

Areial average

A

percipitation = variable so want average (lump model)

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21
Q

methods to average point rainfall data

A
  1. Arithmetic mean
    mean of percipitation gauges but issue is assuming all are the same weight
  2. Thiessen Polygons: wegithed average based on area by connecting stations, perpendicular bisectors and do area*percip/area
  3. Isohyetal method: draw contour lines, and do area times percipitation (contour = take average btwn lines)
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22
Q

Spatial interpolation

A

where no gages find the amount needed
closer values have more influnce than further away

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23
Q

Evaporation process

A

two phases
1. sufficien energy to break through surcae
2. transporation from water surface to atmosphere
occurs when more water turn to gas than back to liquid

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24
Q

Evaporation estimation

A
  1. comparative (pan evaporation)
  2. Aerodnamic method
  3. Balance method
  4. Combination method
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25
Pan evaporation
- free water bodies estimation measure at diff depths Equation: El = KEp
26
Aerodynamic method
from lakes and resvoirs useeses vapor pressure deficit and energy in water Es = water temp Ez = air temp get windspeed at different temperatures find M using formula
27
Energy Balance Method
based on energy received and dissipated by water 1. heat from water to air 2. radiation into water 3. energy from evaporation 4. heat to ground use ratio of sensible to latent and sub in to solve
28
Penman method
Heat + mass problem
29
potentail evapotransperation:
max water that can evaporate and transpire
30
Actual evapotrasnperation
what actually evaporates and transpires, constrainted by availability
31
Refercne crop evaportansperation
the potentail evapotransperation of crop at uniofrmed height, complete covering and growing
32
Crop evapotransperation =
refernce crop and apply crop coefficient
33
method
climate + refercne gets refercne crop evaportaeraptions, Mulitply by factor = crop evapotranperation
34
what affects evapotransperation
1. aerodynamic resistance: function of hieght as more high = more resist 2. Surface resistance function of leaf area and plant height
35
penman-monteith method
2 refercen crops create 2 didferent Kc curves Kc values change in different development stages 4 stages, 3 Kc values Kc1 given by crop evaporation and rain intevals on graph Kc2,Kc3 given by table Stages = initial, development, mid season, late season
36
Runoff
rainfall and in depth NOT STREAMFLOW it is Rain EXCESS or snow after melting
36
irrigation efficiency
based off conveyance (canal lining and length) and application or use of it
37
runoff and inflitration
overtime inflitartion capcity decreaces until a constant rate at this constant rate soil is saturated as this capcaity decreacess the runoff increaces. There is also difference btwn rainfall-runoff and inflitration AFTER RAINFALL ends runoff plummets while infiltration remains the same
38
Determine runoff
horton method or Soil COnservation service
39
Horton method
3 perameter equation to describe function of runoff Fp is drawn on graph, rainfall intensity bar also shown when intensity above Fp = runoff at begininning if less a deficiency occurs after runoff, moisture deficiency is met for later precipitation
40
NRCS method
finding the Curve number is big 1. Get soil group (A,B,C,D) 2. Get moisture condition (I,II,III) 3. Find cover type in table and change it
41
Average curve number
CN times area over area
42
Snowfall
second major percipitation more in mountains where primary is source of water Snowpack: total snow and ice on ground including new and old Snowmelt: converting ice into water with heat
43
Snow characteristics
graph showing snow vs rain chance depneding on temperature 0 certain temp it can only be snow or only be rain, near freezing
44
base temp
if air temp is less than base temp, melt = 0
45
Snow heat sources
solar/longwave atmospheric radiation condensation sensible heat rainwater heat conduction in ground
46
Snow water equivilant
amount of water from certain amount of snow
47
LIquid water content
amount of water in snowpack, snow like soil can be moist, dry, wet
48
Temperature index method
use simple equation given dry vs wet can change the melt coefficent rain on snow can also be consideredd
49
dry vs wet melt rate vs ground melt
dry melt change over year, constant, recongizes that older = melt quicker due to albedo. Wet rain is melt during rain from heat by condesnation/touch ground melt = heat from gorund to snow
50
generalized equations
change depending on conditions heavly forest = 80 forested = 60-80 partly forested = 10-60 open = <10 This is for canopy cover
51
baseflow
baseflow is groundwater flow to streams + interflow(flow of inflitration water travelling to streams above grounlevel) groundwater rsponse time > interflow
52
hydrogrpah
streamflow data showing rate of flow/discharge versus time rising limb = incrase prime andd ouble prime crest = concave down and up/down recession = concave up and decreaseing peak flow = top of crest time base = time during runoff Lage time = time from centroied of percipitation excess to hydrograph centtoid time of conecntration travel time of water from remote point (right most) to the outlet or outflow location
53
baseflow seperation methods
method 1: Join begineering runoff to the end by straight line, if hard to find draw horizontal method 2: recession curve to under peak curve, then connect as straight line to D end of runoff. Calculate N days and find amount after peak Method 3: xtends the recession backwads until point of inflection and then straight line to start
54
Unit Hydrograph
outflow from a single unit of EXCESS rainfall over uniform area at uniform rate. If twice the unit the hydrograph douuhles in y axis. equal excess rainfall equal duration hage same time bases but different discharge
55
using unit graph
multiply the rain in each hour by the increase to total
56
Inverse Procedure developing UH
Steps: 1. need data on rainfall and streamflow 2. near uniform distribution 3. analyze hydrograph and seperate baseflow 4. find total runoff volume and convert to depth 5. Divide runoff hydrograph by excess rainfall depth 6. Determine excess y storm hyetograph
57
Adjust unit hydrograph methods
Lagging method S-Curve Method
58
lagging method:
ONLY INTEGER add together lagged hydrographs and then divide by number lagged UHs
59
S-Cuvve method
used for any duration created by lagging curves over and over before adding together 1. lage curve derivied by t'r 2. subtract the lagged from original 3. multiply by t/t'r
60
Streamflow measurement
the flow of a stream Q = average velocity * cross sectional area LOCATION 50 m upstread/downstream and bed = regular/stable velocities can be 10-15 cm/s aquatic growth can vary
61
Where to measure
depth: 60%, or average of 20 and 80 percent location: different parts that not more than 10-20% total discharge
62
Weirs
measure with V(Smaller) or rectangle, compare discharge rates to water level
63
current meter
put into river ground, measure properllor spinning Gurley meter: propellor to top
64
acoustic doppler current profiler
measure using sound waves, need
65
Non intrusive
infared to mdel
66
tracer
salt water dilution travels based on fact salt is more diljted by a large amount of water than small meausred downstream ideal for hard to measure areas
67
return period/prob of exceedence
return period = years = T average number where equaled is magnitude probability of existance = chance to exceed = P e
68
Weibull method
estimate return period for an event
69
Probobility distribution
distribution of probility of classes
70
Groundwater measure device
metal tape, electric tape, pressurce transducers
71
Groundwater:
water in saturated zone where siol void filled with water, upper boundary is table/level
72
Aquifers
fromations yielding high water, conected by pores or openings water moves with
73
aquifer types
unconfined: supper surface groundwater exposed to atompshere pressure/has water table , confined: more than atmosphere pressure due to layer of medium impermeable
74
Perched aquifers
unconditioned but stratum impermeable existsak
75
leaky
confined that has leak of water out of it
76

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