sandbox/Antoonvh/GABLS1.c

The first GABLS intercomparison case was inspired by the simulations of a stable atmospheric boundary layer over the Arctic ocean by Kosovic and Curry (2000). Image couretesy of pinterest.

The first GABLS intercomparison case was inspired by the simulations of a stable atmospheric boundary layer over the Arctic ocean by Kosovic and Curry (2000). Image couretesy of pinterest.

The GABLS1 case with an adaptive-grid Single Column model

On this page the details of the set-up of for the GABLS1 case are presented. Notice that the code on this page contains many (underlined) hyper links that can be clicked for more information.

General set-up

From the Basilisk source code, we include the so-called `binary-tree-grid’ structure for our computations, the reaction-diffusion equation is solved with the ‘diffusion’ solver and finally, we include the generic timeloop function so that we can time integrate our initial set-up.

#include "grid/bitree.h"
#include "diffusion.h"
#include "run.h"

Closures for turbulent transport.

We use the closures from Louis et al. (1982), Holtslag and Boville (1992) and England and Mcnider (1995) to parameterize the turbulent transport. Their forms are defined below:

#define fris(Ri) (sq((1-(Ri/0.20)))*(Ri<0.20)) //Critical Ri, Short-tail mixing, England and Mcnider (1995)
//#define fris(x) (1/(1+(10*x*(1+8*x)))) // We do not use out-dated Long tail mixing
#define friu(Ri) (sqrt(1-(18*Ri)))            // Holtslag en Boville 1992
#define friubm(Ri,y) ((1-((10*Ri)/(1+75*y*sqrt((x+zo/zo)*fabs(Ri))))))  // Louis 1982
#define friubh(Ri,y) ((1-((15*Ri)/(1+75*y*sqrt((x+zo/zo)*fabs(Ri))))))  // louis 1982

GABLS1 set-up

We use buoyancy as our thermodinamic variable. The surface buoyancy is prescribed by the case according to 0.25K/hour. The surface roughness is set to 10 cm and the maximum level of refinement is set to correspond to 26=64 grid cells. We also declare some variables that will be useful later.

#define bbottom (-0.25/26.5*(t/3600))
 double zo=0.1;
int maxlevel = 6;
mgstats mgb;
int nn;
double Up[100],uu[100],vv[100],bb[100];
double Cm,Ch;
int m = 0;

Among which are the fieds for the velocity components (u,v) and the buoyancy (b);

scalar u[],v[],b[];

We initialize a grid with N=64 cells and set a domain height of 400 metres. After this the simulation starts to run.

int main(){
  init_grid(1<<maxlevel);
  L0=400;
  X0=0;
  run();
}

Boundary Conditions

Here we set so-called no-slip the boundary conditions for the velocity components at the bottom boundary (labelled left), and use the default (stress-free) conditions for the top boundary. For the buoyancy, we set the bottom boundary condition according to the case description and set a Neumann boundary condition consistent with the initialized profile (see next section) at the top boundary (labelled right). Notice that these conditions are only imporant when ghost-cell values need to be read. The surface transport is entirely described by a Monon-Obukhov-type closure that (in our implementation) does not require the definition of ghostcell values (see below).

u[left]=dirichlet(0.);
v[left]=dirichlet(0.);
b[left]=dirichlet(bbottom);
b[right]=neumann(0.01/26.5);

Initialization

The solution is initialized according to the prescribed profiles forto the GABLS1 case (Cuxart et al. 2006). We do this consistently with the adaptive-grid algorithm. We also set the first timestep to be one second.

event init(t=0){
  DT=1.;
  foreach(){
    u[]=8;
    v[]=0;
    b[]=(x>100)*(0.01/26.5)*(x-100);
  }
  boundary(all);
  while(adapt_wavelet({u,v,b},(double[]){0.25,0.25,0.5/26.5},maxlevel,3,{u,v,b}).nc){
    foreach(){
      u[]=8;
      v[]=0;
      b[]=(x>100)*(0.01/26.5)*(x-100);
    }
    boundary(all);
  }
}

Time integration

In this section, time integration is carried out.

event Diffusion(i++){

Therefore we declare the tendency terms due to the Coriolis force and surface transport (rx,ry) for the velocity components (u,v), respectively, and the the tendency field for the buoyancy (rb).

  scalar rx[],ry[],rb[],bf[];

We also declare face vector fields for the turbulent diffusivity (kh), the gradient Richardson number(Ri), the stability correction function (fRi) and a some memory space is allocated to the surface drag coefficient (CN).

  face vector kh[],sqd[],Ri[],fRi[];
  double CN;

On adaptive meshes, face-vectors need to be redefined explicitly before they appear in any computation when a cell is refined.

  kh.x.refine=no_restriction;
  sqd.x.refine=no_restriction;
  Ri.x.refine=no_restriction;
  fRi.x.refine=no_restriction;

We first calculate the tendency term due to the Coriolis force and the geostrophic forcing.

  foreach(){
    rx[]=0.000139*v[];
    rb[]=0;
    ry[]=0.000139*(8-u[]);
For the lowest grid cell, an additional tendency term due to the surface transport is calculated.
    if (x<Delta){

Therefore, we calculate the value of the stability correction function based on the Bulk Richardson number. We distinguish between stable and unstable conditions. Noting that the GABLS1 case is exclusively stable.

      if (b[]>bbottom){
	Cm=sq(0.4/log((x)/zo))*fris(((x-zo)*(b[]-(bbottom))/(sq(u[])+sq(v[]))));
	Ch=Cm;
      }
      else{
	CN =  sq(0.4/log((x)/zo));
	Cm =CN*friubm((x-zo)*(b[]-(bbottom))/(sq(u[])+sq(v[])),CN);
	Ch =CN*friubh((x-zo)*(b[]-(bbottom))/(sq(u[])+sq(v[])),CN);
      }

We `add’ the surface fluxes to the respective tendency terms:

      rx[]-=(u[]*Cm*sqrt(sq(u[])+sq(v[])))/Δ;
      ry[]-=(v[]*Cm*sqrt(sq(u[])+sq(v[])))/Δ;
      rb[]-=((b[]-bbottom)*Cm*sqrt(sq(u[])+sq(v[])))/Δ;
    }
  }

A call the boundary function is adviced so that all cells are in a locally equidistant neighbourhood (see Van Hooft et al. 2018).

  boundary(all);

The turbulent diffusivities (on cell faces) are computed below.

  foreach_face(){

We start out with evaluating the gradient Richardson number on each face.

    sqd.x[]=(sq((u[]-u[-1])/(Delta))+sq((v[]-v[-1])/(Delta)));
    Ri.x[]= ((b[]-b[-1])/(Δ))/(sqd.x[]+0.00001);

That is used to calculate the stability-correction function, using a different formulation for stable and unstable conditions.

    if (Ri.x[]<0)
      fRi.x[]=friu(Ri.x[]);
    else
      fRi.x[]=fris(Ri.x[]);

Finally, kh can be evaluated.

    kh.x[]=sq(min(0.4*x,70))*(sqrt(sqd.x[]))*fRi.x[];
  }

kh should be defined consistently at resolution boundaries.

  boundary({kh.x});

After the timestep dt is set with respect to a maximum timestep DT, the time is advanced by dt with respect to the newly calculted tendencies and difusivities. We log the convergence properties of the interative multigrid scheme that will be used later.

  dt=dtnext(DT);
  mgb=diffusion(u,dt,kh,rx);
  nn+=mgb.i;
  mgb=diffusion(v,dt,kh,ry);
  nn+=mgb.i;
  mgb=diffusion(b,dt,kh,rb);
  nn+=mgb.i;
}

Output

Every ten minutes we output statistics of our simulation. Most notably, the used number of cells and profiles of the used resolution.

event output(t+=360){
  static FILE * fp2 = fopen("GABLScells.dat","w");
  int nnn=0;
  foreach()
    nnn++;
  fprintf(fp2,"%g\t%g\t%d\t%d\n",t,dt,i,nnn);
  fflush(fp2);
  double yp=0;
  static FILE * fp1 = fopen("prfileGABLS10m.dat","w");
  while (yp<400){
    Point point = locate(yp);
    yp=x;
    fprintf(fp1,"%g\t%g\t%g\t%g\t%g\t%d\n",yp,u[],v[],b[],sqrt(sq(u[])+sq(v[])),level);
    yp+=Δ/1.5;
  }
  fflush(fp1);
  
  static FILE * fp5 = fopen("gabls1grid.dat","w");
  for (double mm=0.;mm<=400;mm+=3.125){
    Point point = locate((double)mm);
    fprintf(fp5,"%d\t",level);
  }
  fprintf(fp5,"\n");
  fflush(fp5);
}

Furthermore, in the last hour of simulation averaged profiles are calculated, we do this by evaluating the solution on an equidistant grid using interpolation to 67 points within the domain.

event avgprof(t=8*3600;i+=20)
{
  scalar U[];
  U[left]=dirichlet(0);
  int ng=0;
  foreach(){
    U[]=sqrt(sq(u[])+sq(v[]));
    ng++;
  }
  boundary(all);
  
  static FILE * fp = fopen("prfileGABLS.dat","w");
  double yp=0.;
  int j=0;
  m++;
  while (yp<400)    {
    Up[j]+=interpolate(U,yp);
    uu[j]+=interpolate(u,yp);
    vv[j]+=interpolate(v,yp);
    bb[j]+=interpolate(b,yp);
    if (t==8*3600)
      fprintf(fp,"%g\t%g\t%g\t%g\t%g\n",yp,uu[j]/m,vv[j]/m,bb[j]/m,(Up[j]/(m)));
    j++;
    yp=yp+400./67.;
  }
  fflush(fp);
}

Adaptation

Each timestep the grid is adaptated. Furthermore, the timestep is adapted based on a Vertrouwen-komt-te-voet-en-gaat-the-paard strategy. The simulation is stopped when t=9hours

event adapt(i++;t<=9*3600){
  adapt_wavelet({u,v,b},(double[]){0.25,0.25,0.5/26.5},maxlevel,2,{u,v,b});
  if (nn>14)//Quickly reduce the timestep if things get rough
    DT=max(DT/(1+((double)nn/10.)),1.);
  if (nn<8)//Slowly increase the timestep when time integration is easy.
    DT=min(DT*(1+((double)nn/100.)),15.);
}

Results

Here is a visualization of the output,:

Looks good, we can plot the used number of grid cells over time:

And for the results, we get sensible profiles for wind (u,v) and buoyancy (b), that is now expressed as potential temperature. A low-level jet at approx. 170 m above the surface and with a 9 m/s magnitude is observed. If you wish to lower the low-level jet a bit, one could decrease the value of the critical Richardson number.

Intercomparison of the obtained average profiles over the eigtht hour. The grey shaded region corresponds to the \pm \sigma of the LES results

Intercomparison of the obtained average profiles over the eigtht hour. The grey shaded region corresponds to the ±σ of the LES results

The obtained results correspond very well to the LES results presented by Beare et al. (2006) who performed a LES intercomparison study of the same case. Cuxart et al. (2006) suggested to use the results from these models as a benchmark.

References

Kosović, B., & Curry, J. A. “A large eddy simulation study of a quasi-steady, stably stratified atmospheric boundary layer”. Journal of the atmospheric sciences, 57(8) (2000): 1052-1068.

Beare, Robert J., et al. “An intercomparison of large-eddy simulations of the stable boundary layer.” Boundary-Layer Meteorology 118.2 (2006): 247-272.

Cuxart, Joan, et al. “Single-column model intercomparison for a stably stratified atmospheric boundary layer.” Boundary-Layer Meteorology 118.2 (2006): 273-303.

Holtslag, A. A. M., and B. A. Boville. “Local versus nonlocal boundary-layer diffusion in a global climate model.” Journal of Climate 6.10 (1993): 1825-1842.

Louis, J. “A short history of PBL parameterization at ECMWF.” paper presented at the Workshop on Planetary Boundary Layer Parameterization, Eur. Cent. For Medium-Range Weather Forecasts, Reading, England, 1982. 1982.

England, D. E. and McNider, R. T.: Stability functions based upon shear functions, Boundary-Layer Meteorology, 74, 113–130, 1995.