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9. To control the positioning of the dragged layer, set the following While Dragging options: To keep the layer in its current depth and not bring it to the front when it is dragged, deselect the checkbox for While Dragging: Bring Layer to the Front. To change the stacking order of the layer when it is released, select either Leave on Top or Restore z-order from the drop-down list. 10. To execute a JavaScript command while the layer is being dragged, enter the command or function in the Call JavaScript text box. 11. To execute a JavaScript command when the layer is dropped on the target, enter the code in the When Dropped: Call JavaScript text box. If you want the JavaScript to execute only when the layer is snapped to its target, select the Only if snapped option this option requires that a value be entered in the Snap if Within text box. 12. Click OK when you re done.

(1980) A simpli ed design method and wind tunnel study of horizontal-axis windmills Journal of Wind Engineering and Industrial Aerodynamics 6 pp189 205 Ngo, D & Dexter, A (1999) A robust model-based approach to diagnosing faults in air-handling units ASHRAE Transactions 105(1) pp1078 86 Nielsen, PV (1998) The selection of turbulence models for prediction of room air ow ASHRAE Transactions 104(1B) pp1119 27 Niu, J, vd Kooi, J & vd Ree, H (1997) Cooling load dynamics of rooms with cooled ceilings Building Services Engineering Research & Technology 18(4) pp210 7 Noda, Y, Yamazaki, T, Matsuba, T, Kamimura, K, Kurosu, S (2003) Comparison in control performance between PID and H controllers for HVAC control ASHRAE Transactions 109(1) pp3 11 Norris, LH & Reynolds, WC (1975) Report No FM-10 Stanford University Department of Mechanical Engineering, Stanford, CA.

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the thickness, composition, and pressure temperature pro le of continental crust, which makes ductile ow in its lower parts more likely than it is in oceanic regions The width and diffusivity of these zones make some of the concepts of plate tectonics, such as the rigid motion of plates along narrow boundaries, dif cult to apply to the continents Consequently, the analysis of continental deformation commonly requires a framework that is different to that used to study deformation in oceanic lithosphere (eg Section 85) At the scale of large tectonic features such as wide intracontinental rifts (Section 73), continental transforms (Section 85), and orogenic belts (Section 1043), deformation may be described by a regional horizontal velocity eld rather than by the relative motion of rigid blocks (eg Fig 818b).

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Methods of estimating the regional velocity eld of deforming regions usually involves combining information from Global Positioning System (GPS) satellite measurements (Clarke et al, 1998), fault slip rates (England & Molnar, 1997), and seismicity (Jackson et al, 1992) One of the challenges of this approach is the short, decade-scale time intervals over which GPS data are collected These short intervals typically include relatively few major earthquakes Consequently, the measured surface motions mostly re ect nonpermanent, elastic strains that accumulate between major seismic events (ie interseismic) rather than the permanent strains that occur during ruptures (Bos & Spakman, 2005; Meade & Hager, 2005) This characteristic results in a regional velocity eld that rarely shows the discontinuities associated with slip on major faults.