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Numerical Methods for Time-Dependent DifferentialEquations
Dale DurranUniversity of Washington
22 August 2013
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 1 / 44
Introduction
Broad Categories
ODE’s
PDE’s (emphasizing low-viscosity fluid motion)Spatially discrete
Finite differenceFinite volume
Series expansions
Orthogonal expansion functionsFinite elements
Hybrids
Spectral element and discontinuous Galerkin
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 2 / 44
Introduction
Broad Categories
ODE’sPDE’s (emphasizing low-viscosity fluid motion)
Spatially discreteFinite differenceFinite volume
Series expansionsOrthogonal expansion functionsFinite elements
Hybrids
Spectral element and discontinuous Galerkin
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 2 / 44
Introduction
Broad Categories
ODE’sPDE’s (emphasizing low-viscosity fluid motion)
Spatially discreteFinite differenceFinite volume
Series expansionsOrthogonal expansion functionsFinite elements
HybridsSpectral element and discontinuous Galerkin
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 2 / 44
Introduction
Broad Categories
ODE’sPDE’s (emphasizing low-viscosity fluid motion)
Spatially discreteFinite differenceFinite volume
Series expansionsOrthogonal expansion functionsFinite elements
HybridsSpectral element and discontinuous Galerkin
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 2 / 44
Introduction
Illustrative Equation
Transport in 2D nondivergent flow.
Advective form:∂ψ
∂t+ u
∂ψ
∂x+ v
∂ψ
∂y= 0.
Flux form, an equivalent expression obtained using continuity:
∂ψ
∂t+∂uψ∂x
+∂vψ∂y
= 0.
Flux form facilitates the construction of schemes with local(cell-wise) and global conservation.Advective form helps preserve uniform ψ in non-trivial velocityfields
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 3 / 44
Introduction
Illustrative Equation
Transport in 2D nondivergent flow.
Advective form:∂ψ
∂t+ u
∂ψ
∂x+ v
∂ψ
∂y= 0.
Flux form, an equivalent expression obtained using continuity:
∂ψ
∂t+∂uψ∂x
+∂vψ∂y
= 0.
Flux form facilitates the construction of schemes with local(cell-wise) and global conservation.Advective form helps preserve uniform ψ in non-trivial velocityfields
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 3 / 44
Introduction
Illustrative Equation
Transport in 2D nondivergent flow.
Advective form:∂ψ
∂t+ u
∂ψ
∂x+ v
∂ψ
∂y= 0.
Flux form, an equivalent expression obtained using continuity:
∂ψ
∂t+∂uψ∂x
+∂vψ∂y
= 0.
Flux form facilitates the construction of schemes with local(cell-wise) and global conservation.
Advective form helps preserve uniform ψ in non-trivial velocityfields
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 3 / 44
Introduction
Illustrative Equation
Transport in 2D nondivergent flow.
Advective form:∂ψ
∂t+ u
∂ψ
∂x+ v
∂ψ
∂y= 0.
Flux form, an equivalent expression obtained using continuity:
∂ψ
∂t+∂uψ∂x
+∂vψ∂y
= 0.
Flux form facilitates the construction of schemes with local(cell-wise) and global conservation.Advective form helps preserve uniform ψ in non-trivial velocityfields
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 3 / 44
ODE’s
Basic Theory – ODE’s
Order of accuracy, consistency
Stability + Consistency→ ConvergenceFlavors of stability, A-stable, L-stable
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 4 / 44
ODE’s
Basic Theory – ODE’s
Order of accuracy, consistencyStability + Consistency→ Convergence
Flavors of stability, A-stable, L-stable
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 4 / 44
ODE’s
Basic Theory – ODE’s
Order of accuracy, consistencyStability + Consistency→ ConvergenceFlavors of stability, A-stable, L-stable
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 4 / 44
ODE’s
Basic Method’s – ODE’s
Single-step, single-stage (Forward, Backward Euler, Trapezoidal)
Multistage methods (Runge-Kutta)Multistep methods (Leapfrog, Adams-Bashforth, Backward)
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 5 / 44
ODE’s
Basic Method’s – ODE’s
Single-step, single-stage (Forward, Backward Euler, Trapezoidal)Multistage methods (Runge-Kutta)
Multistep methods (Leapfrog, Adams-Bashforth, Backward)
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 5 / 44
ODE’s
Basic Method’s – ODE’s
Single-step, single-stage (Forward, Backward Euler, Trapezoidal)Multistage methods (Runge-Kutta)Multistep methods (Leapfrog, Adams-Bashforth, Backward)
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 5 / 44
Finite Difference Methods
Theory
General:Order of accuracy, consistency
Stability + Consistency→ ConvergenceStability: Von Neumann, Energy method, CFL condition
Discrete dispersion relationModified equation
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 6 / 44
Finite Difference Methods
Theory
General:Order of accuracy, consistencyStability + Consistency→ Convergence
Stability: Von Neumann, Energy method, CFL condition
Discrete dispersion relationModified equation
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 6 / 44
Finite Difference Methods
Theory
General:Order of accuracy, consistencyStability + Consistency→ ConvergenceStability: Von Neumann, Energy method, CFL condition
Discrete dispersion relationModified equation
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 6 / 44
Finite Difference Methods
Theory
General:Order of accuracy, consistencyStability + Consistency→ ConvergenceStability: Von Neumann, Energy method, CFL condition
For wavelike flows:Discrete dispersion relation
Modified equation
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 6 / 44
Finite Difference Methods
Theory
General:Order of accuracy, consistencyStability + Consistency→ ConvergenceStability: Von Neumann, Energy method, CFL condition
For wavelike flows:Discrete dispersion relationModified equation
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 6 / 44
Finite Difference Methods
Finite difference notation
δnx f (x) =f (x + n∆x/2)− f (x − n∆x/2)
n∆x
Example:
δx fj =fj+ 1
2− fj− 1
2
∆xFlux form with local conservation:
dφi,j
dt+ δx (ui,jφi,j) + δy (vi,jφi,j) = 0
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 7 / 44
Finite Difference Methods
Finite difference notation
δnx f (x) =f (x + n∆x/2)− f (x − n∆x/2)
n∆xExample:
δx fj =fj+ 1
2− fj− 1
2
∆x
Flux form with local conservation:
dφi,j
dt+ δx (ui,jφi,j) + δy (vi,jφi,j) = 0
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 7 / 44
Finite Difference Methods
Finite difference notation
δnx f (x) =f (x + n∆x/2)− f (x − n∆x/2)
n∆xExample:
δx fj =fj+ 1
2− fj− 1
2
∆xFlux form with local conservation:
dφi,j
dt+ δx (ui,jφi,j) + δy (vi,jφi,j) = 0
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 7 / 44
Finite Difference Methods
Finite-Difference Methods
Unknowns are
values at points on a grid: φnj ≈ ψ(j∆x ,n∆t)
Can approximate flux or advective formBasic methods are quite simple:(
dψdx
)j
= δ2xφj+O[(∆x)2],
(dψdx
)j
=43δ2xφj−
13δ4xφj+O[(∆x)4]
More advanced approach: a 4th-order compact scheme (LC)
124
[5(
dψdx
)j+1
+ 14(
dψdx
)j
+ 5(
dψdx
)j−1
]=
112(11δ2xφj + δ4xφj
)
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 8 / 44
Finite Difference Methods
Finite-Difference Methods
Unknowns are values at points on a grid: φnj ≈ ψ(j∆x ,n∆t)
Can approximate flux or advective formBasic methods are quite simple:(
dψdx
)j
= δ2xφj+O[(∆x)2],
(dψdx
)j
=43δ2xφj−
13δ4xφj+O[(∆x)4]
More advanced approach: a 4th-order compact scheme (LC)
124
[5(
dψdx
)j+1
+ 14(
dψdx
)j
+ 5(
dψdx
)j−1
]=
112(11δ2xφj + δ4xφj
)
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 8 / 44
Finite Difference Methods
Finite-Difference Methods
Unknowns are values at points on a grid: φnj ≈ ψ(j∆x ,n∆t)
Can approximate flux or advective form
Basic methods are quite simple:(dψdx
)j
= δ2xφj+O[(∆x)2],
(dψdx
)j
=43δ2xφj−
13δ4xφj+O[(∆x)4]
More advanced approach: a 4th-order compact scheme (LC)
124
[5(
dψdx
)j+1
+ 14(
dψdx
)j
+ 5(
dψdx
)j−1
]=
112(11δ2xφj + δ4xφj
)
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 8 / 44
Finite Difference Methods
Finite-Difference Methods
Unknowns are values at points on a grid: φnj ≈ ψ(j∆x ,n∆t)
Can approximate flux or advective formBasic methods are quite simple:(
dψdx
)j
= δ2xφj+O[(∆x)2],
(dψdx
)j
=43δ2xφj−
13δ4xφj+O[(∆x)4]
More advanced approach: a 4th-order compact scheme (LC)
124
[5(
dψdx
)j+1
+ 14(
dψdx
)j
+ 5(
dψdx
)j−1
]=
112(11δ2xφj + δ4xφj
)
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 8 / 44
Finite Difference Methods
Finite-Difference Methods
Unknowns are values at points on a grid: φnj ≈ ψ(j∆x ,n∆t)
Can approximate flux or advective formBasic methods are quite simple:(
dψdx
)j
= δ2xφj+O[(∆x)2],
(dψdx
)j
=43δ2xφj−
13δ4xφj+O[(∆x)4]
More advanced approach: a 4th-order compact scheme (LC)
124
[5(
dψdx
)j+1
+ 14(
dψdx
)j
+ 5(
dψdx
)j−1
]=
112(11δ2xφj + δ4xφj
)
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 8 / 44
Finite Difference Methods
Phase Speed Error in 1D Advection
Semi-discrete approximation to∂ψ
∂t+ c
∂ψ
∂x= 0.
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 9 / 44
Finite Difference Methods
Utility of High Order
High order schemes converge more rapidly as the grid is refined whenthe solution is already almost correct.
They are essential for efficiency when really trying to converge.Convergence is never achieved in high-Reynolds-number flow.(Why not?)
Exception: all those complicated linear solutions for nontrivial basicstates!
In high-Reynolds-number flow, errors are generally dominated bythe most poorly resolved scales.High-order schemes may treat the marginally resolved scalesbetter.
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 10 / 44
Finite Difference Methods
Utility of High Order
High order schemes converge more rapidly as the grid is refined whenthe solution is already almost correct.
They are essential for efficiency when really trying to converge.
Convergence is never achieved in high-Reynolds-number flow.(Why not?)
Exception: all those complicated linear solutions for nontrivial basicstates!
In high-Reynolds-number flow, errors are generally dominated bythe most poorly resolved scales.High-order schemes may treat the marginally resolved scalesbetter.
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 10 / 44
Finite Difference Methods
Utility of High Order
High order schemes converge more rapidly as the grid is refined whenthe solution is already almost correct.
They are essential for efficiency when really trying to converge.Convergence is never achieved in high-Reynolds-number flow.(Why not?)
Exception: all those complicated linear solutions for nontrivial basicstates!
In high-Reynolds-number flow, errors are generally dominated bythe most poorly resolved scales.High-order schemes may treat the marginally resolved scalesbetter.
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 10 / 44
Finite Difference Methods
Utility of High Order
High order schemes converge more rapidly as the grid is refined whenthe solution is already almost correct.
They are essential for efficiency when really trying to converge.Convergence is never achieved in high-Reynolds-number flow.(Why not?)
Exception: all those complicated linear solutions for nontrivial basicstates!
In high-Reynolds-number flow, errors are generally dominated bythe most poorly resolved scales.High-order schemes may treat the marginally resolved scalesbetter.
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 10 / 44
Finite Difference Methods
Utility of High Order
High order schemes converge more rapidly as the grid is refined whenthe solution is already almost correct.
They are essential for efficiency when really trying to converge.Convergence is never achieved in high-Reynolds-number flow.(Why not?)
Exception: all those complicated linear solutions for nontrivial basicstates!
In high-Reynolds-number flow, errors are generally dominated bythe most poorly resolved scales.
High-order schemes may treat the marginally resolved scalesbetter.
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 10 / 44
Finite Difference Methods
Utility of High Order
High order schemes converge more rapidly as the grid is refined whenthe solution is already almost correct.
They are essential for efficiency when really trying to converge.Convergence is never achieved in high-Reynolds-number flow.(Why not?)
Exception: all those complicated linear solutions for nontrivial basicstates!
In high-Reynolds-number flow, errors are generally dominated bythe most poorly resolved scales.High-order schemes may treat the marginally resolved scalesbetter.
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 10 / 44
Finite Difference Methods
Utility of High Order II
Is it best to approximate all terms with differences having the sameorder of accuracy?
Yes – if you are trying to achieve convergence.Not particularly if you are trying to improve the representation ofpoorly resolved scales.
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 11 / 44
Finite Difference Methods
Utility of High Order II
Is it best to approximate all terms with differences having the sameorder of accuracy?
Yes – if you are trying to achieve convergence.
Not particularly if you are trying to improve the representation ofpoorly resolved scales.
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 11 / 44
Finite Difference Methods
Utility of High Order II
Is it best to approximate all terms with differences having the sameorder of accuracy?
Yes – if you are trying to achieve convergence.Not particularly if you are trying to improve the representation ofpoorly resolved scales.
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 11 / 44
Finite Difference Methods
Example: Staggered Meshes
Arakawa C-grid
um+ 1 , n 2
wm,n+ 1
2
∆z
∆x
Pm,n bm,n
um– 1 , n 2
wm,n– 1
2
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 12 / 44
Finite Difference Methods
Example: Staggered Meshes II
Shallow-water phase speeds using staggered (S) or unstaggered (U) 2nd- or 4th-order differences
0 π/4∆ π/2∆ 3π/4∆ π/∆WAVE NUMBER
50∆ 10∆ 6∆ 4∆ 3∆ 2∆WAVELENGTH
0
c
PHAS
E S
PEED
E
2S
2U4U
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 13 / 44
Finite Difference Methods
Trouble with 2∆x-Waves
Finite-difference methods do not propagate 2∆x-waves on anunstaggered mesh. Why not?
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 14 / 44
Finite Difference Methods
Trouble with 2∆x-Waves
Finite-difference methods do not propagate 2∆x-waves on anunstaggered mesh. Why not?
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 14 / 44
Finite Difference Methods
2∆x-Waves and Negative Group Velocities
Animation of 2∆x-wide spike simulated by upstream and by explicitcentered 2nd and 4th-order finite differences.
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 15 / 44
Finite Difference Methods
2∆x-Waves and Negative Group Velocities
Group velocity is ∂(frequency)∂(wavenumber)
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 16 / 44
Finite Difference Methods
Killing Off 2∆x-Waves
2∆x waves are in serious errorVery short waves can generate aliasing error
Remove the very short waves via:A scale-selective global filter
(Nonlinear) local filters that become active only in regions withlarge-amplitude short-waves
e.g., WENO finite difference methodsMajor focus of finite-volume methods
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 17 / 44
Finite Difference Methods
Killing Off 2∆x-Waves
2∆x waves are in serious errorVery short waves can generate aliasing error
Remove the very short waves via:A scale-selective global filter
(Nonlinear) local filters that become active only in regions withlarge-amplitude short-waves
e.g., WENO finite difference methodsMajor focus of finite-volume methods
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 17 / 44
Finite Difference Methods
Killing Off 2∆x-Waves
2∆x waves are in serious errorVery short waves can generate aliasing error
Remove the very short waves via:A scale-selective global filter(Nonlinear) local filters that become active only in regions withlarge-amplitude short-waves
e.g., WENO finite difference methodsMajor focus of finite-volume methods
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 17 / 44
Finite Difference Methods
Killing Off 2∆x-Waves
2∆x waves are in serious errorVery short waves can generate aliasing error
Remove the very short waves via:A scale-selective global filter(Nonlinear) local filters that become active only in regions withlarge-amplitude short-waves
e.g., WENO finite difference methods
Major focus of finite-volume methods
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 17 / 44
Finite Difference Methods
Killing Off 2∆x-Waves
2∆x waves are in serious errorVery short waves can generate aliasing error
Remove the very short waves via:A scale-selective global filter(Nonlinear) local filters that become active only in regions withlarge-amplitude short-waves
e.g., WENO finite difference methodsMajor focus of finite-volume methods
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 17 / 44
Finite Volume Methods
Finite Volume Methods
Unknowns are cell averages:
φnj ≈
1∆x
∫ xj +∆x/2
xj−∆x/2ψ(x ,n∆t) dx
Essential for the simulation of shocksWeak solutions satisfy integral form of conservation law
Approximations most naturally in flux formFluxes at cell boundaries computed from sub-cell reconstructionsLeads directly to two-level forward-in-time schemes
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 18 / 44
Finite Volume Methods
Finite Volume Methods
Unknowns are cell averages:
φnj ≈
1∆x
∫ xj +∆x/2
xj−∆x/2ψ(x ,n∆t) dx
Essential for the simulation of shocksWeak solutions satisfy integral form of conservation law
Approximations most naturally in flux formFluxes at cell boundaries computed from sub-cell reconstructionsLeads directly to two-level forward-in-time schemes
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 18 / 44
Finite Volume Methods
Finite Volume Methods
Unknowns are cell averages:
φnj ≈
1∆x
∫ xj +∆x/2
xj−∆x/2ψ(x ,n∆t) dx
Essential for the simulation of shocksWeak solutions satisfy integral form of conservation law
Approximations most naturally in flux form
Fluxes at cell boundaries computed from sub-cell reconstructionsLeads directly to two-level forward-in-time schemes
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 18 / 44
Finite Volume Methods
Finite Volume Methods
Unknowns are cell averages:
φnj ≈
1∆x
∫ xj +∆x/2
xj−∆x/2ψ(x ,n∆t) dx
Essential for the simulation of shocksWeak solutions satisfy integral form of conservation law
Approximations most naturally in flux formFluxes at cell boundaries computed from sub-cell reconstructions
Leads directly to two-level forward-in-time schemes
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 18 / 44
Finite Volume Methods
Finite Volume Methods
Unknowns are cell averages:
φnj ≈
1∆x
∫ xj +∆x/2
xj−∆x/2ψ(x ,n∆t) dx
Essential for the simulation of shocksWeak solutions satisfy integral form of conservation law
Approximations most naturally in flux formFluxes at cell boundaries computed from sub-cell reconstructionsLeads directly to two-level forward-in-time schemes
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 18 / 44
Finite Volume Methods
Sub-Cell Reconstructions
f
x0 2π
f
x0 2π
(a)
(b)
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 19 / 44
Finite Volume Methods
Avoiding overshoots and undershoots
When it it important?
When simulating shocks. Consistent monotonemethods in flux form converge to the entropy consistent solution.
φn+1j = H(φn
j−p, . . . , φnj+q+1),
is monotone if∂ H(φj−p, . . . , φj+q+1)
∂φi≥ 0
for each integer i in the interval [j − p, j + q+1].
Monotone schemesDo not produce spurious ripples.Are first-order accurate.
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 20 / 44
Finite Volume Methods
Avoiding overshoots and undershoots
When it it important? When simulating shocks. Consistent monotonemethods in flux form converge to the entropy consistent solution.
φn+1j = H(φn
j−p, . . . , φnj+q+1),
is monotone if∂ H(φj−p, . . . , φj+q+1)
∂φi≥ 0
for each integer i in the interval [j − p, j + q+1].
Monotone schemesDo not produce spurious ripples.Are first-order accurate.
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 20 / 44
Finite Volume Methods
Avoiding overshoots and undershoots
When it it important? When simulating shocks. Consistent monotonemethods in flux form converge to the entropy consistent solution.
φn+1j = H(φn
j−p, . . . , φnj+q+1),
is monotone if∂ H(φj−p, . . . , φj+q+1)
∂φi≥ 0
for each integer i in the interval [j − p, j + q+1].
Monotone schemesDo not produce spurious ripples.Are first-order accurate.
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 20 / 44
Finite Volume Methods
Avoiding overshoots and undershoots
When it it important? When simulating shocks. Consistent monotonemethods in flux form converge to the entropy consistent solution.
φn+1j = H(φn
j−p, . . . , φnj+q+1),
is monotone if∂ H(φj−p, . . . , φj+q+1)
∂φi≥ 0
for each integer i in the interval [j − p, j + q+1].
Monotone schemesDo not produce spurious ripples.Are first-order accurate.
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 20 / 44
Finite Volume Methods
Advection of a Step Function
0.5 1 0.5 1x x
(a) (b)
Left: 2nd-order centered with global 4th-derivative smoother
Right: Upstream and Lax-Friedrichs (red) monotone methods
Strategy: Scheme becomes monotone near discontinuities and ishigh-order elsewhere.
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 21 / 44
Finite Volume Methods
Advection of a Step Function
0.5 1 0.5 1x x
(a) (b)
Left: 2nd-order centered with global 4th-derivative smoother
Right: Upstream and Lax-Friedrichs (red) monotone methods
Strategy: Scheme becomes monotone near discontinuities and ishigh-order elsewhere.
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 21 / 44
Finite Volume Methods
Avoiding overshoots and undershoots
When is it important in problems without shocks?
Chemically reactingflow
∂ψ1
∂t+ c
∂ψ1
∂x= −rψ1ψ2,
∂ψ2
∂t+ c
∂ψ2
∂x= rψ1ψ2.
ψ1
ψ2
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 22 / 44
Finite Volume Methods
Avoiding overshoots and undershoots
When is it important in problems without shocks? Chemically reactingflow
∂ψ1
∂t+ c
∂ψ1
∂x= −rψ1ψ2,
∂ψ2
∂t+ c
∂ψ2
∂x= rψ1ψ2.
ψ1
ψ2
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 22 / 44
Finite Volume Methods
Avoiding overshoots and undershoots
When is it important in problems without shocks? Chemically reactingflow
∂ψ1
∂t+ c
∂ψ1
∂x= −rψ1ψ2,
∂ψ2
∂t+ c
∂ψ2
∂x= rψ1ψ2.
ψ1
ψ2
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 22 / 44
Finite Volume Methods
Avoiding overshoots and undershoots
When is it important in problems without shocks? Chemically reactingflow
∂ψ1
∂t+ c
∂ψ1
∂x= −rψ1ψ2,
∂ψ2
∂t+ c
∂ψ2
∂x= rψ1ψ2.
ψ1
ψ2
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 23 / 44
Finite Volume Methods
Minmod limiter
One local-smoothing strategy to prevent growth of ripples.
x
φ~
If sgn(φj+1 − φj) 6= sgn(φj − φj−1) slope in cell j is zeroOtherwise | slope | is min(|φj+1 − φj |, |φj − φj−1|)
Scheme is TVD, but not monotone.
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 24 / 44
Finite Volume Methods
Minmod limiter
One local-smoothing strategy to prevent growth of ripples.
x
φ~
If sgn(φj+1 − φj) 6= sgn(φj − φj−1) slope in cell j is zeroOtherwise | slope | is min(|φj+1 − φj |, |φj − φj−1|)
Scheme is TVD, but not monotone.
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 24 / 44
Finite Volume Methods
Limiters in Action
Minmod (long-dashed), MC (red), Superbee (short-dashed)
(a) (b)
2 3x
0 30∆x
Nice job at jump, but messes up smooth extremum.
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 25 / 44
Finite Volume Methods
Limiters in Action
Minmod (long-dashed), MC (red), Superbee (short-dashed)
(a) (b)
2 3x
0 30∆x
Nice job at jump, but messes up smooth extremum.
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 25 / 44
Finite Volume Methods
Order of Accuracy
Scheme Estimated Order of AccuracyUpstream 0.9
Minmod Limiter 1.6Superbee Limiter 1.6
Zalesak FCT 1.7MC Limiter 1.9
Lax–Wendroff 2.0
Table: Empirically determined order of accuracy for constant-wind-speedadvection of a sine wave
Avoid limiting smooth extrema!
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 26 / 44
Finite Volume Methods
Order of Accuracy
Scheme Estimated Order of AccuracyUpstream 0.9
Minmod Limiter 1.6Superbee Limiter 1.6
Zalesak FCT 1.7MC Limiter 1.9
Lax–Wendroff 2.0
Table: Empirically determined order of accuracy for constant-wind-speedadvection of a sine wave
Avoid limiting smooth extrema!
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 26 / 44
Spectral Methods
Orthogonal Expansion Functions
Unknowns are coefficients of expansion functions ak (t)
φ(x , t) =N∑
k=1
ak (t)ϕk (x)
Evolution equations for ak obtained viaGalerkin requirement that residual be orthogonal to all ϕk (x)
“Spectral"Global conservation of φ and φ2
Collocation requirement that sets the residual to zero at a set ofgrid points
“Pseudo-spectral"50% faster than spectralLose conservation
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 27 / 44
Spectral Methods
Orthogonal Expansion Functions
Unknowns are coefficients of expansion functions ak (t)
φ(x , t) =N∑
k=1
ak (t)ϕk (x)
Evolution equations for ak obtained viaGalerkin requirement that residual be orthogonal to all ϕk (x)
“Spectral"Global conservation of φ and φ2
Collocation requirement that sets the residual to zero at a set ofgrid points
“Pseudo-spectral"50% faster than spectralLose conservation
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 27 / 44
Spectral Methods
Orthogonal Expansion Functions
Unknowns are coefficients of expansion functions ak (t)
φ(x , t) =N∑
k=1
ak (t)ϕk (x)
Evolution equations for ak obtained viaGalerkin requirement that residual be orthogonal to all ϕk (x)
“Spectral"Global conservation of φ and φ2
Collocation requirement that sets the residual to zero at a set ofgrid points
“Pseudo-spectral"50% faster than spectralLose conservation
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 27 / 44
Spectral Methods
Orthogonal Expansion Functions – II
Using orthogonal expansion functionsDecouples the evolution equations for the ak (good for explicit timedifferencing).
Computation of the forcing for all N of the ak involves O(N2)operations (Fourier methods can be O(N log N)).
Jan 2010: ECMWF refines to T1279
“Spectral accuracy" when approximating smooth functions — errorgoes to zero faster than any finite power of the effective gridspacing.Not conducive to preserving positivity or treating steep gradients
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 28 / 44
Spectral Methods
Orthogonal Expansion Functions – II
Using orthogonal expansion functionsDecouples the evolution equations for the ak (good for explicit timedifferencing).Computation of the forcing for all N of the ak involves O(N2)operations (Fourier methods can be O(N log N)).
Jan 2010: ECMWF refines to T1279
“Spectral accuracy" when approximating smooth functions — errorgoes to zero faster than any finite power of the effective gridspacing.Not conducive to preserving positivity or treating steep gradients
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 28 / 44
Spectral Methods
Orthogonal Expansion Functions – II
Using orthogonal expansion functionsDecouples the evolution equations for the ak (good for explicit timedifferencing).Computation of the forcing for all N of the ak involves O(N2)operations (Fourier methods can be O(N log N)).
Jan 2010: ECMWF refines to T1279
“Spectral accuracy" when approximating smooth functions — errorgoes to zero faster than any finite power of the effective gridspacing.
Not conducive to preserving positivity or treating steep gradients
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 28 / 44
Spectral Methods
Orthogonal Expansion Functions – II
Using orthogonal expansion functionsDecouples the evolution equations for the ak (good for explicit timedifferencing).Computation of the forcing for all N of the ak involves O(N2)operations (Fourier methods can be O(N log N)).
Jan 2010: ECMWF refines to T1279
“Spectral accuracy" when approximating smooth functions — errorgoes to zero faster than any finite power of the effective gridspacing.Not conducive to preserving positivity or treating steep gradients
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 28 / 44
Spectral Methods
Global Overshoots and Undershoots with PoorResolution
(b)(a)
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 29 / 44
Spectral Methods
Finite Element Methods
Piecewise linear elements (chapeau functions)
x0 2π
0
16
0
17
0
15
0
18
0
13
0
14
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 30 / 44
Spectral Methods
The Galerkin Requirement
General PDE∂ψ
∂t+ F (ψ) = 0
The residual isR(φ) =
∂φ
∂t+ F (φ)
If the residual is orthogonal to every expansion function ϕk (x),
N∑n=1
Mn,kdan
dt= −
∫S
[F( N∑
n=1
anϕn
)ϕk
]dx for all k = 1, . . . ,N
The mass matrix isMn,k =
∫Sϕnϕk dx
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 31 / 44
Spectral Methods
The Galerkin Requirement
General PDE∂ψ
∂t+ F (ψ) = 0
The residual isR(φ) =
∂φ
∂t+ F (φ)
If the residual is orthogonal to every expansion function ϕk (x),
N∑n=1
Mn,kdan
dt= −
∫S
[F( N∑
n=1
anϕn
)ϕk
]dx for all k = 1, . . . ,N
The mass matrix isMn,k =
∫Sϕnϕk dx
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 31 / 44
Spectral Methods
The Galerkin Requirement
General PDE∂ψ
∂t+ F (ψ) = 0
The residual isR(φ) =
∂φ
∂t+ F (φ)
If the residual is orthogonal to every expansion function ϕk (x),
N∑n=1
Mn,kdan
dt= −
∫S
[F( N∑
n=1
anϕn
)ϕk
]dx for all k = 1, . . . ,N
The mass matrix isMn,k =
∫Sϕnϕk dx
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 31 / 44
Spectral Methods
The Galerkin Requirement
General PDE∂ψ
∂t+ F (ψ) = 0
The residual isR(φ) =
∂φ
∂t+ F (φ)
If the residual is orthogonal to every expansion function ϕk (x),
N∑n=1
Mn,kdan
dt= −
∫S
[F( N∑
n=1
anϕn
)ϕk
]dx for all k = 1, . . . ,N
The mass matrix isMn,k =
∫Sϕnϕk dx
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 31 / 44
Finite Element Methods
Finite Element Methods
Expansion functions have compact support
N∑n=1
Mn,kdan
dt= −
∫S
[F( N∑
n=1
anϕn
)ϕk
]dx
Evaluation of the RHS for all N of the ak involves only O(N)operations.The evolution equations for the ak are coupled
Implicit solve every time stepVery inefficient for wave-propagation problems
Implicit coupling in quadratic or cubic finite element methodsmakes them completely impractical for the simulation of waves.Higher-order finite element methods are the nevertheless thestandard approach for solving may elliptic problems.
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 32 / 44
Finite Element Methods
Finite Element Methods
Expansion functions have compact support
N∑n=1
Mn,kdan
dt= −
∫S
[F( N∑
n=1
anϕn
)ϕk
]dx
Evaluation of the RHS for all N of the ak involves only O(N)operations.The evolution equations for the ak are coupled
Implicit solve every time stepVery inefficient for wave-propagation problems
Implicit coupling in quadratic or cubic finite element methodsmakes them completely impractical for the simulation of waves.Higher-order finite element methods are the nevertheless thestandard approach for solving may elliptic problems.
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 32 / 44
Finite Element Methods
Finite Element Methods
Expansion functions have compact support
N∑n=1
Mn,kdan
dt= −
∫S
[F( N∑
n=1
anϕn
)ϕk
]dx
Evaluation of the RHS for all N of the ak involves only O(N)operations.
The evolution equations for the ak are coupledImplicit solve every time stepVery inefficient for wave-propagation problems
Implicit coupling in quadratic or cubic finite element methodsmakes them completely impractical for the simulation of waves.Higher-order finite element methods are the nevertheless thestandard approach for solving may elliptic problems.
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 32 / 44
Finite Element Methods
Finite Element Methods
Expansion functions have compact support
N∑n=1
Mn,kdan
dt= −
∫S
[F( N∑
n=1
anϕn
)ϕk
]dx
Evaluation of the RHS for all N of the ak involves only O(N)operations.The evolution equations for the ak are coupled
Implicit solve every time stepVery inefficient for wave-propagation problems
Implicit coupling in quadratic or cubic finite element methodsmakes them completely impractical for the simulation of waves.Higher-order finite element methods are the nevertheless thestandard approach for solving may elliptic problems.
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 32 / 44
Finite Element Methods
Finite Element Methods
Expansion functions have compact support
N∑n=1
Mn,kdan
dt= −
∫S
[F( N∑
n=1
anϕn
)ϕk
]dx
Evaluation of the RHS for all N of the ak involves only O(N)operations.The evolution equations for the ak are coupled
Implicit solve every time stepVery inefficient for wave-propagation problems
Implicit coupling in quadratic or cubic finite element methodsmakes them completely impractical for the simulation of waves.
Higher-order finite element methods are the nevertheless thestandard approach for solving may elliptic problems.
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 32 / 44
Finite Element Methods
Finite Element Methods
Expansion functions have compact support
N∑n=1
Mn,kdan
dt= −
∫S
[F( N∑
n=1
anϕn
)ϕk
]dx
Evaluation of the RHS for all N of the ak involves only O(N)operations.The evolution equations for the ak are coupled
Implicit solve every time stepVery inefficient for wave-propagation problems
Implicit coupling in quadratic or cubic finite element methodsmakes them completely impractical for the simulation of waves.Higher-order finite element methods are the nevertheless thestandard approach for solving may elliptic problems.
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 32 / 44
Finite Element Methods
Finite Element versus Compact Differencing in 1D
1D advection equation∂ψ
∂t+ c
∂ψ
∂x= 0
Piecewise linear finite-elements:
ddt
(aj+1 + 4aj + aj−1
6
)+ c
(aj+1 − aj−1
2∆x
)= 0
4th-order compact scheme:
dφj
dt+ c
(dψdx
)j
= 0
16
[(dψdx
)j+1
+ 4(
dψdx
)j
+
(dψdx
)j−1
]=φj+1 − φj−1
2∆x
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 33 / 44
Finite Element Methods
Finite Element versus Compact Differencing in 1D
1D advection equation∂ψ
∂t+ c
∂ψ
∂x= 0
Piecewise linear finite-elements:
ddt
(aj+1 + 4aj + aj−1
6
)+ c
(aj+1 − aj−1
2∆x
)= 0
4th-order compact scheme:
dφj
dt+ c
(dψdx
)j
= 0
16
[(dψdx
)j+1
+ 4(
dψdx
)j
+
(dψdx
)j−1
]=φj+1 − φj−1
2∆x
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 33 / 44
Finite Element Methods
Finite Element versus Compact Differencing in 1D
1D advection equation∂ψ
∂t+ c
∂ψ
∂x= 0
Piecewise linear finite-elements:
ddt
(aj+1 + 4aj + aj−1
6
)+ c
(aj+1 − aj−1
2∆x
)= 0
4th-order compact scheme:
dφj
dt+ c
(dψdx
)j
= 0
16
[(dψdx
)j+1
+ 4(
dψdx
)j
+
(dψdx
)j−1
]=φj+1 − φj−1
2∆x
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 33 / 44
Finite Element Methods
Finite Element versus Compact Differencing in 1D
Schemes are identical!
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 34 / 44
Finite Element Methods
Finite Element versus Compact Differencing in 2D
4th-order compact scheme:
dφi,j
dt+ u
(dψdx
)i,j
+ v(
dψdy
)i,j
= 0
16
[(dψdx
)i+1,j
+ 4(
dψdx
)i,j
+
(dψdx
)i−1,j
]=φi+1,j − φi−1,j
2∆x
16
[(dψdy
)i,j+1
+ 4(
dψdy
)i,j
+
(dψdy
)i,j−1
]=φi,j+1 − φi,j−1
2∆y
Finite-elements: huge implicit mess (element couples with itself and 8neighbors).
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 35 / 44
Finite Element Methods
Finite Element versus Compact Differencing in 2D
4th-order compact scheme:
dφi,j
dt+ u
(dψdx
)i,j
+ v(
dψdy
)i,j
= 0
16
[(dψdx
)i+1,j
+ 4(
dψdx
)i,j
+
(dψdx
)i−1,j
]=φi+1,j − φi−1,j
2∆x
16
[(dψdy
)i,j+1
+ 4(
dψdy
)i,j
+
(dψdy
)i,j−1
]=φi,j+1 − φi,j−1
2∆y
Finite-elements: huge implicit mess (element couples with itself and 8neighbors).
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 35 / 44
Hybrid Methods
The Challenge
How do weExtend finite-volume methods to high order (beyond piecewiseparabolic or cubic)?
Extend finite-element methods to high order while avoiding implicitcoupling (and other bad behaviors)?Avoid the global coupling and O(N2) operation counts to update aset of expansion coefficients in spectral or pseudo-spectralmethods?
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 36 / 44
Hybrid Methods
The Challenge
How do weExtend finite-volume methods to high order (beyond piecewiseparabolic or cubic)?Extend finite-element methods to high order while avoiding implicitcoupling (and other bad behaviors)?
Avoid the global coupling and O(N2) operation counts to update aset of expansion coefficients in spectral or pseudo-spectralmethods?
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 36 / 44
Hybrid Methods
The Challenge
How do weExtend finite-volume methods to high order (beyond piecewiseparabolic or cubic)?Extend finite-element methods to high order while avoiding implicitcoupling (and other bad behaviors)?Avoid the global coupling and O(N2) operation counts to update aset of expansion coefficients in spectral or pseudo-spectralmethods?
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 36 / 44
Hybrid Methods
One Solution
Use h-p methods – break domain into h elements and represent thesolution within each element by orthogonal polynomials of maximumorder p.
Spectral element methods – solution is continuous at cellboundaries (good for approximating 2nd-order derivatives).Discontinuous Galerkin methods – solution is discontinuousacross cell boundaries (localizes communication between cells).
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 37 / 44
Hybrid Methods
One Solution
Use h-p methods – break domain into h elements and represent thesolution within each element by orthogonal polynomials of maximumorder p.
Spectral element methods – solution is continuous at cellboundaries (good for approximating 2nd-order derivatives).
Discontinuous Galerkin methods – solution is discontinuousacross cell boundaries (localizes communication between cells).
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 37 / 44
Hybrid Methods
One Solution
Use h-p methods – break domain into h elements and represent thesolution within each element by orthogonal polynomials of maximumorder p.
Spectral element methods – solution is continuous at cellboundaries (good for approximating 2nd-order derivatives).Discontinuous Galerkin methods – solution is discontinuousacross cell boundaries (localizes communication between cells).
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 37 / 44
Hybrid Methods
Discontinuous Galerkin Method
Enforce Galerkin criterion locally, within each element.
Two flavors of DG. Polynomial structure within each element is eitherModal: Legendre polynomials
Nodal: Lagrange polynomials interpolating theGauss-Legendre-Lobatto (GLL) points
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 38 / 44
Hybrid Methods
Discontinuous Galerkin Method
Enforce Galerkin criterion locally, within each element.
Two flavors of DG. Polynomial structure within each element is eitherModal: Legendre polynomials
Nodal: Lagrange polynomials interpolating theGauss-Legendre-Lobatto (GLL) points
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 38 / 44
Hybrid Methods
Discontinuous Galerkin Method
Enforce Galerkin criterion locally, within each element.
Two flavors of DG. Polynomial structure within each element is eitherModal: Legendre polynomialsNodal: Lagrange polynomials interpolating theGauss-Legendre-Lobatto (GLL) points
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 38 / 44
Hybrid Methods
Modal DG
First 5 Legendre Polynomials
(a)-1 -0.5 0 0.5 1
-1
-0.5
0
0.5
1
-0.5
Truly orthogonal
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 39 / 44
Hybrid Methods
Nodal DG
Lagrange Polynomials Interpolating 5 GLL Nodes
(b)-1 -0.5 0 0.5 1
-0.5
0
0.5
1
Discrete orthogonality using quadrature at the nodes
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 40 / 44
Hybrid Methods
DG Considerations
Advantages:Suitable for massively parallel computing
Communicates via fluxes with nearest neighbors onlyFor high order-polynomials, solution relatively insensitive to fluxformulationLots of work to do within each element
Rapid convergence for smooth solutions
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 41 / 44
Hybrid Methods
DG Considerations
Advantages:Suitable for massively parallel computing
Communicates via fluxes with nearest neighbors only
For high order-polynomials, solution relatively insensitive to fluxformulationLots of work to do within each element
Rapid convergence for smooth solutions
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 41 / 44
Hybrid Methods
DG Considerations
Advantages:Suitable for massively parallel computing
Communicates via fluxes with nearest neighbors onlyFor high order-polynomials, solution relatively insensitive to fluxformulation
Lots of work to do within each element
Rapid convergence for smooth solutions
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 41 / 44
Hybrid Methods
DG Considerations
Advantages:Suitable for massively parallel computing
Communicates via fluxes with nearest neighbors onlyFor high order-polynomials, solution relatively insensitive to fluxformulationLots of work to do within each element
Rapid convergence for smooth solutions
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 41 / 44
Hybrid Methods
DG Considerations
Advantages:Suitable for massively parallel computing
Communicates via fluxes with nearest neighbors onlyFor high order-polynomials, solution relatively insensitive to fluxformulationLots of work to do within each element
Rapid convergence for smooth solutions
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 41 / 44
Hybrid Methods
DG Considerations II
Disadvantages:Requires very short time step
Grid spacing reduced toward element boundaries
DiscontinuitiesCan be accommodated across element boundaries by limiting thefluxes
Cannot naturally be accommodated within each element
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 42 / 44
Hybrid Methods
DG Considerations II
Disadvantages:Requires very short time step
Grid spacing reduced toward element boundariesDiscontinuities
Can be accommodated across element boundaries by limiting thefluxes
Cannot naturally be accommodated within each element
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 42 / 44
Hybrid Methods
DG Considerations II
Disadvantages:Requires very short time step
Grid spacing reduced toward element boundariesDiscontinuities
Can be accommodated across element boundaries by limiting thefluxesCannot naturally be accommodated within each element
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 42 / 44
Coda
Closing Opinions
The practical distinction between finite-difference andfinite-volume methods is most consequential in (particularly whensplitting along each spatial dimension)
In the simulation of shocks!In the time differencing.
“Spectral convergence" is hard to beat if the solution is smooth.When simulating low-viscosity flow, finite elements are tooinefficient except for irregular geometriesh-p methods hold great promise, but rely on massively parallelcomputers to be competitive.
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 43 / 44
Coda
Closing Opinions
The practical distinction between finite-difference andfinite-volume methods is most consequential in (particularly whensplitting along each spatial dimension)
In the simulation of shocks!In the time differencing.
“Spectral convergence" is hard to beat if the solution is smooth.
When simulating low-viscosity flow, finite elements are tooinefficient except for irregular geometriesh-p methods hold great promise, but rely on massively parallelcomputers to be competitive.
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 43 / 44
Coda
Closing Opinions
The practical distinction between finite-difference andfinite-volume methods is most consequential in (particularly whensplitting along each spatial dimension)
In the simulation of shocks!In the time differencing.
“Spectral convergence" is hard to beat if the solution is smooth.When simulating low-viscosity flow, finite elements are tooinefficient except for irregular geometries
h-p methods hold great promise, but rely on massively parallelcomputers to be competitive.
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 43 / 44
Coda
Closing Opinions
The practical distinction between finite-difference andfinite-volume methods is most consequential in (particularly whensplitting along each spatial dimension)
In the simulation of shocks!In the time differencing.
“Spectral convergence" is hard to beat if the solution is smooth.When simulating low-viscosity flow, finite elements are tooinefficient except for irregular geometriesh-p methods hold great promise, but rely on massively parallelcomputers to be competitive.
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 43 / 44
Coda
Reference
Durran, D.R., 2010: Numerical Methods for Fluid Dynamics: WithApplications to Geophysics. 2nd Ed. Springer.
Dale Durran (Atmospheric Sci.) Amath 586 Review University of Washington 44 / 44