program info_RSC94 

      implicit double precision (a-h,o-z)
      logical in_sol,pseudo,rad
      dimension time(2),rlat(2),rlon(2),u(3,2),v(3,2)

c...Read sample input data file to get time and position. 
c    rlat - north latitude (in degrees, -90 to  90)
c    rlon - east longitude (in degrees,  0  to 360)
c    time - desired time,  Modified Julian Date in days. e.g.,
c     Jan 1, 1992 is 48622.

      rlat(1) = -65.44040
      rlon(1) = 277.80185
      time(1) = 49354.41959

      rlat(2) = -63.10150
      rlon(2) = 291.97490
      time(2) = 49354.50178

      do i = 1,2
c...Convert time to seconds desired by the model
      time(i) = time(i)*86400.d0

c...Call RSC94 model to compute the tide height
c       in_sol - logical denoting whether tide data exists
c                at desired location
c       tpd    - computed ocean tide height(ocean+load) in cm
c       tld    - long period tide in cm        
c       tide   - predicted ocean tide in cm

      call tptide(rlat(i),rlon(i),time(i),tpd,in_sol,u,v,pseudo,rad)

c...Compute the long period tide height
      call lpeqmt (time(i),rlat(i),tld)

       tide = tpd + tld

      if (in_sol) then
        write(6,*) rlat(i),rlon(i),time(i),tide,tpd,tld
      else
        write(6,*) 'No tide solution avaliable.'
      endif

      enddo

      stop
      end 

c...The output data is:
c   -65.44040, 277.80185, 4264221852.576004, 22.06897, 24.37343, -2.30446
c   -63.10150, 291.97490, 4264228953.792007, 31.08258, 33.27571, -2.19313


c  RSC94
c  -----
c       This model (version 941230) was briefly described in an  abstract
c  by  Ray  et  al. [1994]; (although the last sentence of that abstract,
c  referring to use of 250 gauge data, does not apply to this version  of
c  the  model).   The  model was derived by a generalized response method
c  [Groves and  Reynolds,  1975]  and,  with  the  response  weights  (or
c  orthoweights)  expressed  by  expansions  in Proudman functions (up to
c  maximum degree 700).  Hence,  the  model  was  created  by  one  large
c  inversion   problem,  of  approximate  size  5300  coefficients.   The
c  Proudman functions were computed on a 1-degree grid covering the  area
c  between  latitudes  !-68!   and  68 ,  although several marginal areas
c  (e.g., the Mediterranean,  Hudson  Bay,  and  the  complex  seas  near
c  Indonesia)  were  excluded.  The additional radiational forcing at the
c  !S2! frequency was handled by the method suggested by  Cartwright  and
c  Ray  [1994].   The model is completely independent of any other model;
c  i.e., it is not a correction to some previous model.   (This  is  also
c  true  of  the Desai-Wahr and Egbert-Bennett-Foreman models.)  However,
c  for this version, the Cartwright-Ray model was used for the  load-tide
c  correction.

c       The tidal solution was based on repeat cycles 1 to 64, with  both
c  TOPEX  and  POSEIDON  contributing. (A relative bias between these two
c  altimeters was estimated simultaneously with the tidal  coefficients.)
c  Additionally, the harmonic constants at about 20 stations were used in
c  the inversion; most of these stations are located along the  perimeter
c  of  the  Labrador  Sea,  where ice cover often yielded fewer altimeter
c  observations, and the North Sea.