imbrie {astrochron} | R Documentation |

An implementation of the Imbrie and Imbrie (1980) ice sheet model

imbrie(insolation=NULL,Tm=17,b=0.6,times=NULL,initial=0,burnin=100,standardize=T, output=T,genplot=1,verbose=T)

`insolation` |
Insolation, in ka (negative for future, positive for past). Default is insolation over the past 1000 ka from 65 deg. North, 21 June. |

`Tm` |
Vector of mean time constants in ka. Default is 17 ka. The order of the Tm values should match vectors b and times. |

`b` |
Vector of nonlinearity coefficient (a value ranging from 0 to 1). Default is 0.6. The order of the b values should match vectors Tm and times. |

`times` |
Vector of start times for each Tm and b listed above. Leave as NULL if you only need to model one Tm and b value. |

`initial` |
Initial value for ice volume, relative to centered record. Default is 0. |

`burnin` |
Number of points for model burn-in. This is required to achieve stable model results. Default is 100 points. |

`standardize` |
Standardize model output to maximum value of one and minimum value of zero? (T or F) |

`output` |
Output model results? (T or F) |

`genplot` |
Generate summary plots? (1) plot insolation and ice volume series, (2) plot animated insolation, ice volume and phase portrait.) |

`verbose` |
Verbose output? (T or F) |

This function will implement the ice volume model of Imbrie and Imbrie (1980), following the conventions of Paillard et al. (1996).

When using the 'times' vector, consider the following example:

times= c(500,1000)

Tm=c(15,5)

b=c(0.6,0.3)

In this case, a Tm of 15 (b of 0.6) will be applied to model from 0-500 ka, and a Tm of 5 (b of 0.3) will be applied to model 500-1000 ka.

Imbrie, J., and Imbrie, J.Z., (1980),
*Modeling the Climatic Response to Orbital Variations*: Science, v. 207, p. 943-953.

Lisiecki, L. E., and M. E. Raymo, 2005,
*A Pliocene-Pleistocene stack of 57 globally distributed benthic d18O records*, Paleoceanography, 20, PA1003, doi:10.1029/2004PA001071.

Paillard, D., L. Labeyrie and P. Yiou, (1996),
*Macintosh program performs time-series analysis*: Eos Trans. AGU, v. 77, p. 379.

## Not run: # make a very simple forcing (on/off) forcing=cycles(0,end=300) forcing[50:150,2]=1 plot(forcing,type="l") # use this forcing to drive the imbrie ice model # set b=0, Tm = 1 imbrie(forcing,b=0,Tm=1,output=F) # let's view the evolution of the ice sheet imbrie(forcing,b=0,Tm=1,output=F,genplot=2) # now increase the response time imbrie(forcing,b=0,Tm=10,output=F,genplot=2) # now model slow growth, fast decay imbrie(forcing,b=0.5,Tm=10,output=F,genplot=2) # now make a 100 ka cyclic forcing forcing=cycles(1/100,end=300) imbrie(forcing,b=0,Tm=1,output=F,genplot=2) imbrie(forcing,b=0,Tm=10,output=F,genplot=2) imbrie(forcing,b=0.5,Tm=10,output=F,genplot=2) # show burn-in imbrie(forcing,b=0.5,Tm=10,output=F,genplot=2,burnin=0) # now examine Malutin Milankovitch's hypothesis: 65 deg N, summer solstice imbrie(b=0.5,Tm=10,output=F,genplot=2,burnin=900) # use the ice model output to make a synthetic stratigraphic section res=imbrie(b=0.5,T=10,output=T,genplot=1,burnin=100) synthStrat(res,clip=F) # generate ice model for last 5300 ka, using 65 deg. N insolation, 21 June # allow b and Tm values to change as in Lisiecki and Raymo (2005): insolation=getLaskar("insolation") insolation=iso(insolation,xmin=0,xmax=5300) # b is 0.3 from 5300 to 3000 ka, then linearly increases to 0.6 between 3000 and 1500 ka. # b is 0.6 from 1500 ka to present. set_b=linterp(cb(c(1500,3000),c(0.6,0.3)),dt=1) set_b=rbind(set_b,c(5400,0.3)) # Tm is 5 ka from 5300 to 3000 ka, then linearly increases to 15 ka between 3000 and 1500 ka. # Tm is 15 ka from 1500 ka to present. set_Tm=linterp(cb(c(1500,3000),c(15,5)),dt=1) set_Tm=rbind(set_Tm,c(5400,5)) # now run model ex=imbrie(insolation=insolation,Tm=set_Tm[,2],b=set_b[,2],times=set_b[,1]) # time-frequency analysis of model result eha(ex,fmax=0.1,win=500,step=10,pad=5000,genplot=4,pl=2) ## End(Not run)

[Package *astrochron* version 1.0 Index]