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The main objective of the report is to present the overall communication network structure for the Advanced Solid Rocket Motor (ASRM) facility being built at Yellow Creek near Iuka, Mississippi. This report is compiled using information received from NASA/MSFC, LMSC, AAD, and RUST Inc. As per the information gathered, the overall network structure will have one logical FDDI ring acting as a backbone for the whole complex. The buildings will be grouped into two categories viz. manufacturing critical and manufacturing non-critical. The manufacturing critical buildings will be connected via FDDI to the Operational Information System (OIS) in the main computing center in B 1000. The manufacturing non-critical buildings will be connected by 10BASE-FL to the Business Information System (BIS) in the main computing center. The workcells will be connected to the Area Supervisory Computers (ASCs) through the nearest manufacturing critical hub and one of the OIS hubs. The network structure described in this report will be the basis for simulations to be carried out next year. The Comdisco's Block Oriented Network Simulator (BONeS) will be used for the network simulation. The main aim of the simulations will be to evaluate the loading of the OIS, the BIS, the ASCs, and the network links by the traffic generated by the workstations and workcells throughout the site.

The propagation of planetary waves between the troposphere and stratosphere is investigated using a linear, time-dependent, primitive equation model. It is found that the tropopause acts like a valve for the propagation of planetary waves. The key parameters controlling the valve are the vertical gradient of buoyancy frequency and the vertical shear of the zonal winds at the tropopause. For a given wind profile smaller gradient of buoyancy frequency enhances the propagation of planetary waves. For a given profile of buoyancy frequency the larger the shear, the more the wave activity is trapped in the troposphere, and therefore, there is less left to propagate into the stratosphere. The transmission across the tropopause is, however, not sensitive to zonal winds in the upper stratosphere. The propagation of planetary waves is very sensitive to transience. More transient waves propagate more vertically within the troposphere, and for more transient waves, more wave activity is transferred into the stratosphere from the troposphere.

A linear, time-dependent, primitive-equation, 3D numerical model is used to investigate the dynamical coupling between the troposphere and stratosphere through the vertical propagation of planetry waves. Attention is given to the roles of the tropopause in affecting the propagation of planetary waves and to the extent to which the stratosphere can determine its own wave driving, i.e., the sensitivity of the generation of the wave activity in the troposphere to the change of zonal wind in the stratosphere. Two maxima in Eliassen-Palm (EP) flux convergence are found for wave 1 in high latitudes, one in the upper stratosphere and the other in the upper troposphere. For wave 2 there is a third maximum north of the zero wind line in the tropical stratosphere. The formation of the maximum in EP-flux convergence in the upper troposphere is related to the dissipation of non-WKBJ waves near a local maximum of the refractive index. The existence of the local maximum in refractive index at the tropopause is a result of the great gradient of the buoyancy frequency as well as the vertical shear of the zonal flow there.

The propagation of planetary-scale Rossby waves in the stratosphere is investigated in a linear, time-dependent, primitive equation model. Two distinct maxima in the convergence of the Eliassen-Palm flux (EP flux) are found for steady and for transient waves in a variety of realistic northern hemisphere, winter season, zonal flows; one below the stratospheric polar jet and the other north of the zero wind line. These maxima appear at higher altitudes for wave 1 than for wave 2, especially in low latitudes. Different mechanisms cause the formation of these two maxima. The confinement of wave activity in high latitudes is mainly due to the dissipation of waves in that region under non-WKBJ conditions. The maximum in lower latitudes is related to the absorption of Rossby waves near their critical lines. For wave 2, the intensity of the high latitude maximum is sensitive to the transience of the wave forcing at the tropopause, while for wave 1 this sensitivity is reduced. For both waves the low latitude maximum shifts northward with increasing transience.