<Dl> <Dd> h (t) = h 0 + α e f f ∫ 0 ∞ (T (z) − T 1) d z = h 0 − 2 π α e f f T 1 κ t (\ displaystyle h (t) = h_ (0) + \ alpha _ (\ mathrm (eff)) \ int _ (0) ^ (\ infty) (T (z) - T_ (1)) dz = h_ (0) - (\ frac (2) (\ sqrt (\ pi))) \ alpha _ (\ mathrm (eff)) T_ (1) (\ sqrt (\ kappa t))) </Dd> </Dl> <Dd> h (t) = h 0 + α e f f ∫ 0 ∞ (T (z) − T 1) d z = h 0 − 2 π α e f f T 1 κ t (\ displaystyle h (t) = h_ (0) + \ alpha _ (\ mathrm (eff)) \ int _ (0) ^ (\ infty) (T (z) - T_ (1)) dz = h_ (0) - (\ frac (2) (\ sqrt (\ pi))) \ alpha _ (\ mathrm (eff)) T_ (1) (\ sqrt (\ kappa t))) </Dd> <P> where α e f f (\ displaystyle \ alpha _ (\ mathrm (eff))) is the effective volumetric thermal expansion coefficient, and h is the mid-ocean ridge height (compared to some reference). </P> <P> Note that the assumption the v is relatively large is equivalently to the assumption that the thermal diffusivity κ (\ displaystyle \ kappa) is small compared to L 2 / T (\ displaystyle L ^ (2) / T), where L is the ocean width (from mid-ocean ridges to continental shelf) and T is its age . </P>

Where do seafloors with older ages tend to be found