Lecture-1: FVCOM-An unstructured grid Finite-Volume ... · FVCOM-An unstructured grid Finite-Volume...
Transcript of Lecture-1: FVCOM-An unstructured grid Finite-Volume ... · FVCOM-An unstructured grid Finite-Volume...
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Lecture-1:
FVCOM-An unstructured grid Finite-Volume Community Ocean Model
Chen-FVCOM-2013-01-Chile
Changsheng Chen School for Marine Science and Technology University of Massachusetts-Dartmouth New Bedford, MA 02744 Email: [email protected], [email protected] Website: http://fvcom.smast.umassd.edu
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Critical Issues in Coastal Ocean Modeling
Irregular geometry
Intertidal wetlands
Steep topography
Mass Conservation ?
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Critical Issues for Global Ocean:
u Multi-scale dynamics: Basin-shelf interaction, convection via advection, etc.
u Resolving irregular coastal geometries connected to the North Atlantic Ocean and Pacific Ocean
Basin scale Basin-shelf interaction
Coastal process
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Chen-FVCOM-2013-01-Chile
1. Finite-volume algorithms: Configuring the computational domains with individual control volumes and calculating the variables by a net flux through control volumes
Possible solutions:
( ) ( ) Ddsvdxdy]yDv
xDu[dxdy
t Sn∫∫∫∫∫ −=
∂
∂+
∂
∂−=
∂
∂ζAn example:
2. Unstructured grids: Configuring the computational domains with unstructured grids to provide the accurate fitting of the irregular coastal geometry.
An example:
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FVCOM: Unstructured-grid, Finite-Volume Coastal Ocean Model (Chen, C. R. H. Liu and R. C. Beardsley, JAOT, 2003)
• All variables are computed in the integral form of the equations, which provides a better representation of the conservative laws of mass, momentum and heat in the coastal region with complex geometry. • The numerical computational domain consists of non-overlapping unstructured cells.
• Combines the best from the finite-element method for the geometric flexibility and finite difference method for the simplest discrete computation.
• Both current and tracer remain the second-order accuracy.
u,v
u,v
u,v
u,v
u,v
u,v F
F F
F
F F
F
etcKKHSTF hm ,,,,,,,: !"
yʹ′
u,v
u,v u,v
u,v
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: H, !, ", D, s, #, q2, q2l, Am, Kh I : u, v,
For example: The Continuity Equation:
( ) ( )Ddsvdxdy]
yDv
xDu
[dxdyt S
n!!!!! "=#
#+
#
#"=
#
#$
!
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FVCOM Wet/Dry Treatment Technology-Coastal Inundation
ζ
u, v
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Spherical Coordinate at the Arctic
In the Cartesian coordinates,
!! ==ss
dydx 0;0 A line integral is closed
North Pole
0cos !"s
dr #$
In the spherical coordinates,
A line integral is not always closed
!"!""# dddrr s
$$$ %&&
'(
)( cos2 ?
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Spherical Coordinate FVCOM
u,vcosϕ
F
u,vcosϕ
u,vcosϕ
u,vcosϕ
u,vcosϕ
u,vcosϕ
0)cos(cos1
=!
!+
!!
+!!
""
#"$ DvDu
rt
F: Scalar variables such as ζ, T, S, Km, Kh,..and vertical velocity ω. • : The node of triangles where scalar variable or vertical velocity is calculated ⊗: The centroid of a triangle where the horizontal velocity is calculated.
Example: Continuity equation
0cos)cos(cos1cos 22 =
!!
+!!
+!!
""""##
$%$$$
%$$%$
& ddrDvDur
ddrt
])cos()([! !"#"=
$$
%&&' dvDduDrt
u,vcosϕ
T
T T
T
T T
T
u,vcosϕ
u,vcosϕ u,vcosϕ
u,vcosϕ
u,vcosϕ The gradient of the water temperature (or salinity) is determined by the Green’s function through the integration over the larger volume (with boundaries linked to nodes).
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Treatment of North Pole
Centroid calculated using the polar stereographic projection coordinate.
Centroid calculated directly in the spherical coordinate system.
Node calculated directly in the spherical coordinate system.
Node calculated using the polar stereographic projection coordinate.
!!"
#$$%
&!!"
#$$%
&
'
''=!!
"
#$$%
&
s
s
p
p
vu
vu
((
((
sincoscossin
2sin12sin1
!
!
+==
+==
yyp
xxp
hdtdy
hv
hdtdx
hu
Conversion formulae between (up, vp) and (us, vs):
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FVCOM-Main Code Cartesian/Spherical Coordinates
Modules of FVCOM 3-D Wet/Dry Treatment
General Ocean Turbulence Model
(GOTM)
3-D Sediment Model
Generalized Biological Model
Water Quality Models
Multi OB Radiations
Forcings: Tides (Equilibrium+ O.B.) Winds, Heat flux, Precipitation/Evaporation River discharges, Groundwater O.B. fluxes
Lagrangian-IBM
MPI Parallel
NetCDF Output
GUI Post-process Tools Ice model
Nudging/OI Assimilation
Ensemble/Reduced Kalman Filters
North Pole Nested System
Adjoint Assimilation
Surface Wave Model
Model Field Sampling
Multiple Nesting
ViSiT Monitoring
Existing Modules Under Development Key:
Non-hydrostatic
Solver: Mode-split or semi-implicit; 2-D and 3-D, Types: Research version (FVCOM-v2.7) and Forecast version (FVCOM-v3.1).
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ViSiT Software developed by Lawrence Livermore National Laboratory
http://www.llnl.gov/visit/ • Open source; Parallel visualization; Interactive simulation support • Multiple platform support (LINUX, UNIX, PC, MAC)
FVCOM Plug-in for VISIT • FVCOM NETCDF files • Visualization and animation of 3D vector and scalar fields • Database linking to NETCDF formatted particle tracking output
Example of density isosurfaces from a high resolution FVCOM GOM model
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Australia, Bangladesh, Brazil, Canada, Chile, China, Colombia, Denmark, Egypt, France, Germany, Hong Kong, Hungary India, Indonesia, Iran, Israel, Italy, Jamaica, Japan, Korea, Kuwait, Malaysia, Mexico, Netherlands, New Zealand, Norway Peru, Saudi Arabia, Singapore, Sweden, Taiwan, Thailand, Turkey, U.S., UK, Venezuela, Vietnam
FVCOM Users 38 countries(including HK/Taiwan) >1000 users or institutions
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Hydrostatic FVCOM Validation Experiments
1. Advection scheme;
2. Wind-induced oscillation (POM, ECOM-si);
3. Wind-induced waves over the slope bottom topography (POM, ECOM-si);
4. Tidal Resonances in a semi-enclosed channel and a sector (POM, ECOM-si);
5. Freshwater discharge plume (POM, ECOM-si);
6. Bottom boundary layer over a step bottom slope (POM; ECOM-si)
7. Equatorial Rossby soliton (ROMs)
8. Wind-induced lateral boundary (ROMs)
9. Super-critical current (ROMs)
Non-Hydrostatic FVCOM Validation Experiments
1. Standing surface short gravity waves; 2. Lock exchanges; 3. Solitary waves in both homogeneous and layer fluids.
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!F!t
+C !F!x
= 0
1. Advection Scheme
F (x,0) =5, !2 " x " 2
0, otherwise
#
$%
&%
and C = 1
Upwind finite-difference stream
Central finite-difference stream
FVCOM finite-volume flux scheme
Δt = 0.05, Δx=0.1
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Upwind finite-difference stream
Central finite-difference stream
FVCOM finite-volume flux scheme
Δt = 0.005, Δx=0.01
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0])([ =∂
∂+
∂
∂+
∂
∂
∂
∂−=+
∂
∂
∂
∂−=−
∂
∂
θλζ
θζ
λ
ζλ
vrru
rt
ru
tv
rv
tu
ro=67.5 km
d=75 m
Wind Linear, non-dimensional equations:
Wind-induced oscillation
where
and
!(r,! ,t) = ! o! 4[Ao (r)cos! + akAk (r)cos(! !" kt)]
k=1
"
#
u(r,! ,t) = ! o!3[(Ao (r)r
!1)sin! ! bkk=1
"
# Fk (r)sin(! !" kt)]
v(r,! ,t) = ! o!3[(dAo (r)dr
!1)cos! ! bkk=1
"
# Gk (r)cos(! !" kt)]
Solution:
Wind is suddenly imposed at initial
Reference: Csanady ( 1968) Birchfield (1969)
!
" =gdro f
;# =$ % ˆ $ ; ˆ $ =& orcos'
"4 ;& o =g&ro
3 f 4
!
u r=1 = 0; (u,v,")r=0 # finite; u t=0 = v t=0 = 0;" t=0 = $ ˆ % (r,& )
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Unstructured (FVCOM) Structured (POM)
Chen-FVCOM-2013-01-Chile
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Water elevation Alongshore transport
Chen-FVCOM-2013-01-Chile
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Chen-FVCOM-2013-01-Chile
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Chen-FVCOM-2013-01-Chile
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Birchfield and Hickie (1977) JPO
Radial mode: k=1, 2: gravity waves, k=3: topographic wave
Analytical FVCOM (5 km) POM (2.5 km)
1 h
1 d
Chen-FVCOM-2013-01-Chile
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FVCOM (5 km) POM (2.5 km) 5 days
ζ: Elevation
: Currents V
Chen-FVCOM-2013-01-Chile
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Chen-FVCOM-2013-01-Chile
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Chen-FVCOM-2013-01-Chile
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Structured (POM) Unstructured (FVCOM)
Chen-FVCOM-2013-01-Chile
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Structured (POM)
Unstructured (FVCOM)
Chen-FVCOM-2013-01-Chile
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Tidal Resonance in A Semi-closed Channel
0=∂∂
+∂∂
rg
tVr η 0=
∂∂
+∂∂
θηθ
rg
tV
Consider a 2-D linear, non-rotated initial problem such as
000 =∂
∂+
∂
∂+
∂∂
θη θ
rHV
rrHrV
tr{
The solution:
])2/(cos[)]()([),(0
20
10 ααθπωω
θη γγ
+⋅+=
mgH
rYcgH
rJcrmm
)()()()(/[)(00
1'
01
'
001
'1 gH
LYgH
LJgH
LYgH
LJgH
LYAcmmmmm
ωωωωωγγγγγ −⋅=
)()()()(/[)(00
1'
01
'
001
'2 gH
LYgH
LJgH
LYgH
LJgH
LJAcmmmmm
ωωωωωγγγγγ −⋅−=
απγ /mm =
where
Chen-FVCOM-2013-01-Chile
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1. Normal condition (non-resonance)
2. Near-resonance condition
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A Normal Case
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A Near-resonance Case
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Near-resonance, 2 km (FVCOM), 1 km (POM&ECOM-si)
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Near-resonance, 2km, Curvilinear
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0.5-4 km
4 km
2 km
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Slope topography fitting
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Equatorial Rossby Soliton L = 48
D = 24
C=0.4
Periodic boundary condition
1. Nonlinear shallow water equation in equatorial β-plane
2. Inviscid flow
3. Asymptotic solutions available to zero and first orders
(Boyd 1980,1985)
Grid A
Grid B
Grid C
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Grid A
Grid B
Grid C
0.5
0.25 0.125 0.05
Δx (ND)
FVCOM (2nd)
ROMS (4th)
SEOM (7-9th)
hn/ht Cn/Ct hn/ht Cn/Ct hn/ht Cn/Ct
0.5 0.472 0.917 0.884 1.088 0.923 0.98
0.25 0.846 0.984 0.926 0.993 0.929 0.99
0.125 0.92 0.984 0.923 0.986 0.937 0.989
0.05 0.935 0.983 0.936 0.983 0.915 0.98
hn: Computed peak of the sea surface elevation at 120 units ht: Analytical peak of the sea surface elevation at 120 units Cn: Computed average speed Ct
: Analytical averaged speed.
Comments: 1. Analytical solution only represents the zero and
1st modes, while the numerical solution contains a complete set of higher order modes. This is not surprised to see numerical models can not exactly reach the analytical solutions.
2. FVCOM shows a fast convergence with increase of horizontal resolution.
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• Barotropic shallow water equations
• No rotation considered, i.e. f =0, β = 0
• Steady analytical solutions for u, ζ and the jump angle relative to the x axis.
(m)
No gradient condition Hydraulic Jump
(m) φ = 8.95o
00
/57.8
===
!v
scmu
30o
Characteristics:
Maximum sea level: Minimum sea level: Mean sea level: Mean velocity: Mean Froude #: Shock angle: Thickness: Mean deviation:
Analytical solution:
m5.0max =!
m0min =!
m5.0=mean!
075.2==gDuFr
030=!
m0=!
m0=dy
m/su 956.7=
Chen-FVCOM-2013-01-Chile
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∆x = 0.5 m, ∆t = 0.002
The case with no horizontal diffusion: FVCOM quickly reaches steady status.
∆x = 0.25 m, ∆t = 0.001 ∆x = 0.125 m, ∆t = 0.0005
Model grids ∆t ζmax ζmin ζmean ū Fr α δ |dy|
True 0.5 0 0.5 7.956 2.075 30 0 0
FVCOM 80 X 60
0.002 0.688 -0.269 0.5 7.949 2.072 29.952 0.111 0.305
160 X 120 0.001 0.697 -0.268 0.499 7.951 2.073 30.030 0.063 0.151
320 X240 0.0005 0.696 -0.272 0.5 7.951 2.073 30.029 0.037 0.076
ROMs Reach an oscillatory solution without horizontal diffusion.
Chen-FVCOM-2013-01-Chile
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Over shocking can be reduced by introducing a slope limiter method (Hubbard, J. Comput. Phys., 1999).
Original code Modified code with limiter
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3-Dimensional Wind-Driven Flow in an Elongated, Rotating Basin Winant (J. Phys. Oceano. 2004)
where X(x) is a function in the form of
∆x is a constant specified as 0.3% of the total length of the basin.
)]})/(1)(/([92.008.0{ 20 ByLxXhh !"+=
ByBLxL !!"!!" ,
!"
!#$
%&'%
%+&&
%&<= xx
xxx
xxxX 1||,]1||[1
1||,1)( 2
Length: 2L; width: 2B, and bathymetry:
x
y
z
2L
!"
!#
$
%%
+&'=(
=+)&
2
2
0
zvKgvkf
wv
m
z!
!!
!
*
!"
!#$
%===
===
hzatwv
zatwK
vm
sz
00
00r
rr&
'
B.Cs:
Steady status analytical solution for this linear equation system is given as:
])cosh()cosh(
1[)cosh()](sinh[
2 hzi
hhz
ivu yx
!!
!
""
!!!
#+
#+
=+
dzvw y!"=
where α2 = 2iδ-2 and δ = (2E)1/2 (E: Ekman number).
Governing equations:
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Analytic
FVCOM
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V W U
Be aware that ROMs underestimates u and overestimates w (color bar scales are different for analytical and ROMs’ solutions). This figure is scanned from Winant’s working note.
Analytic
ROMs
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A non-hydrostatic problem: Lock-exchange flow
Heavy fluid Light fluid
0.8m
0.1m
Model setup: • Initially • Vertical 100 sigma layers • Horizontal 400×5 nodes, dx = 0.002(m) • no bottom friction and viscosity/diffusivity
20 /01.0/' smgg =Δ= ρρ
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Chen-FVCOM-2013-01-Chile
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Kinetic Energy (KE )= 12!V (u2 + v2 )dxdz
0
H
!"L/2
L/2
!
Under an inviscid condition, the total energy is conservative at an order of 10-4.
Blue line: PE
Red line: KE
Potential Energy (PE ) = !gz dxdz0
H
!"L/2
L/2
!
Is the total energy conservative?
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FVCOM-NH
Comparison of FVCOM-NH with a high-order direct numerical simulation (DNS) method, with constant horizontal and vertical eddy viscosity and tracer diffusivity 1×10-6 m2/s:
(DNS results from Härtel et al., 2000)
ROMS’s results presented by Kanarska et al. ( 2007)
SUNTRAN’s results presented by Fringer et al. (2006) with a first-order finite-volume scheme.
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Internal solitary waves breaking on a linear varying slope
1ρ
2ρH
h
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Photography (Michallet and Ivey ,1999) FVCOM-NH
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Photography (Michallet and Ivey ,1999) FVCOM-NH
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53
Under shear instability condition
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Under the vortex condition
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55
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References
Chen, C. H. Liu, R. C. Beardsley, 2003. An unstructured, finite-volume, three-dimensional, primitive equation ocean model: application to coastal ocean and estuaries. Journal of Atmospheric and Oceanic Technology, 20, 159-186. Chen, C, R. C. Beardsley and G. Cowles, 2006. An unstructured grid, finite-volume coastal ocean model (FVCOM) system. Special Issue entitled “Advance in Computational Oceanography”, Oceanography, 19(1), 78-89. Chen, C. H. Huang, R. C. Beardsley, H. Liu, Q. Xu and G. Cowles, 2007. A finite-volume numerical approach for coastal ocean circulation studies: comparisons with finite difference models. Journal of Geophysical. Research. 112, C03018, doi:10.1029/2006JC003485. Huang, H, C. Chen, G. W. Cowles, C. D. Winant, R. C. Beardsley, K. S. Hedstrom and D. B Haidvogel, 2008. FVCOM validation experiments: comparisons with ROMS for three idealized barotropic test problems. J. Geophys. Res., 113, C07042, doi: 10.1029/2007JC004557. Lai, Z., C. Chen, G. Cowles, and R. C. Beardsley, 2010. A Non-Hydrostatic Version of FVCOM, Part I: Validation Experiments, J. Geophys. Res.-Oceans, 115, doi:10.1029/2009JC005525.