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The following comes straight from a tutorial by Ian Tickle which is distributed in postscript form as $CDOC/Iso_repl_itickle_tut.bath.ps. There is now also an HTML version of this tutorial.

**2. Scaling.**

**2.1. Background.**

Two CCP4 programs are available for determining and applying the scale factor(s)
of the derivative dataset(s) relative to the reference native dataset: **SCALEIT** and
**FHSCAL**. In accordance with the CCP4 philosophy of accumulating all reflection
data in one file, the datasets must be contained within different columns in the same
file (column-merging of files is accomplished with the **MTZUTILS** program).

It should be realised however that the FHSCAL program is designed specifically for
derivative-to-native scaling, whereas SCALEIT is more general purpose, and can also
be used for scaling of observed to calculated structure factor amplitudes. FHSCAL
uses the "**Kraut**" scaling procedure, which is inherently more accurate than the
"**Wilson**" and/or **least squares** procedure used by SCALEIT.
Another difference is
that SCALEIT uses one formula to fit all the scale factors, whereas FHSCAL divides
the data into resolution shells, smooths the shell scale factors and then interpolates
to get the final scale factor for each reflection.
A third option is "**local**" scaling, where
each reflection gets an individual scale factor which only depends on the relative
scales of the reflections in its immediate neighbourhood.

Usually these differences are not important because initially only a rough scale factor
is needed for the isomorphous difference Patterson, and the scale factor is refined
later along with the heavy-atom parameters (*i.e.* 3-D coordinates, site occupancies,
individual isotropic and/or anisotropic thermal parameters), and the relative overall
thermal parameter for each derivative. SCALEIT has a very useful extra feature, the
display of **Normal probability analysis plots** that can be used to decide whether the
observed isomorphous and anomalous differences are really significant, or just due
to errors in the measurements.

**2.2. Scaling procedures.**

The "Kraut" and "Wilson" scale factors are derived by considering the origin peak
heights of the native (*F*_{P}),
derivative (*F*_{PH}) and
heavy-atom (*F*_{H}) Patterson maps. Any
point in a Patterson represents a vector, and the Patterson density at the point equals
the sum of products of pairs of electron densities at points in the unit cell of the
crystal that are separated by that vector. So the Patterson origin peak represents the
sum of squares of electron densities in the unit cell. Because of the **Fourier transform**
relationship between the Patterson and the **measured intensities**
(= amplitude^{2} ), the
Patterson origin peak height is simply the sum of squares of the corresponding
amplitudes (this is basically Wilson's equation).

Provided the derivative structure is obtained simply by summing the native and
heavy-atom structures, in other words that it is perfectly **isomorphous**, the derivative
Patterson origin peak is just the sum of the native and heavy-atom Patterson origin
peaks. Of course, the "heavy-atom structure" exists only in the imagination, as it
consists only of heavy atoms in the same position as in the derivative structure, but
otherwise completely empty space. Consequently we have:

S(*k*
|*F*_{PH}| )^{2} =
S
|*F*_{P}|^{2} +
S
|*F*_{H}|^{2}

Here *k* is the unknown scale factor needed to multiply all the measured derivative
amplitudes to put them on the same scale as the measured native amplitudes. Both
are of course on completely arbitrary scales, because the X-ray experiment does not
take into account the incident beam intensity, crystal size, wavelength, and all the
other factors that one would need to know to calculate absolute diffracted intensities.
Consequently, **all** structure factors and occupancies in subsequent calculations are
scaled relative to the arbitrarily scaled native amplitudes. This is an important point
to grasp; if you don't, you will be baffled later on by occupancies greater than 1!

The heavy-atom amplitudes |*F*_{H}| are of course
completely unknown at this stage, and because they are on average smaller than
|*F*_{P}| or
|*F*_{PH}|,
a possible assumption
is simply to assume that they do not make a significant contribution and to ignore
them; this gives the "Wilson" scale factor:

*k*_{Wilson} =
Ö
( S
|*F*_{P}|^{2} /
S
|*F*_{PH}|^{2} )

Alternatively, the heavy-atom amplitude can be estimated from the
**isomorphous difference**:
| *k* |*F*_{PH}| -
|*F*_{P}| |.
In fact, except for weak reflections where we may get
a **cross-over** such that
|*F*_{H}| = *k* |*F*_{PH}| + |*F*_{P}|,
in the case of **centric** reflections (where
the phase can only take 1 of 2 values differing by 180° so the complex structure
factors are collinear), they are the same. For the remaining **acentric** reflections, which
are almost always the majority, because the unknown native and heavy-atom phases
are uncorrelated, it can be shown that the average isomorphous difference squared
is half the average
|*F*_{H}|^{2}.
It is of course this fact that will allow us to use the
**isomorphous difference Patterson** as an approximation to the
**heavy-atom Patterson**.
These relationships allow the unknown
S |*F*_{H}|^{2}
term to be eliminated, rather than
ignored, so a more accurate estimate of the scale factor
*k*_{Kraut} is obtained from the
resulting quadratic. For full details of the algebra, consult the FHSCAL program
documentation.

Finally, the least-squares estimate of the scale factor is obtained by minimising the
sum of weighted squares of isomorphous differences:
S *w* (*k* |*F*_{PH}| - |*F*_{P}| )^{2} with
respect to the unknown scale factor, where *w* is a weight equal to the reciprocal
variance of the isomorphous difference:
*w* = 1/((*k* s_{PH})^{2} + s_{P}^{2} ).
However, the inherent
assumption is again that the |*F*_{H}|
can be ignored;
in practice this introduces an error
of 5-10% in the scale factor, which may affect correct interpretation of the Patterson.

To illustrate the effect of the heavy atoms on the scale factor, consider a small protein
of 1000 atoms (assume for simplicity they are all N atoms). The mean scattering
intensity of the protein
<|*F*_{P}|^{2}>
will be proportional to 1000x7² = 49000. If a single
mercury atom is then introduced it will contribute 80² = 6400, so the fractional mean
intensity difference between native and derivative will be 6400/49000 = 0.13.

In practice, because the introduction of the heavy atoms into the protein can
anisotropically increase the disorder in the crystal, and also because of effects like
absorption of X-rays by the heavy atoms, the relative scale factor can vary both with
resolution and in direction, and so the procedure is a little more complicated.
Programs may therefore have the option of applying an overall relative isotropic or
anisotropic temperature factor to the
|*F*_{PH}|'s,
or of applying scale factors either in
equi-volume shells or in localised regions of reciprocal space.