具有单向强耦合的时滞大系统的稳定性

针对具有单向强耦合的时滞大系统,通过构造Lyapunou泛函,并采用部分分解法,给出了判定系统一致渐近稳定的充分条件。与传统的分解等价法相比,该方法扩大了单方向关联项的界限,并可通过参数的选取扩大时滞界限,结论易于验证,具有实际应用价值。     

具有Leakage变时滞的脉冲反应扩散神经网络的鲁棒指数稳定性

研究一类具有Leakage变时滞和不确定参数的脉冲反应扩散神经网络的平衡点的鲁棒指数稳定性。所研究模型中的Leakage时滞为变时滞,脉冲既与神经元当前状态有关,又与Leakage时滞和传输时滞所产生的历史状态有关。利用Lyapunov函数、Razumikhin技巧和线性矩阵不等式(LMI)方法获得了系统鲁棒指数稳定的新的判别条件。最后给出一个实例说明结果的有效性和实用性。     

时滞不确定随机系统的鲁棒稳定性

主要研究了带有时滞的不确定随机系统的均方鲁棒指数稳定性问题。根据有关线性矩阵不等式理论,结合李亚普诺夫函数法,充分利用系统的扩散项,建立了1个新的时滞相关稳定判据,使文中的时滞不确定随机系统是鲁棒均方指数稳定的。给出了具体的数值例子说明了研究结果的可行性和有效性。     

时滞不确定随机系统的鲁棒稳定性

主要研究了带有时滞的不确定随机系统的均方鲁棒指数稳定性问题.根据有关线性矩阵不等式理论,结合李亚普诺夫函数法,充分利用系统的扩散项,建立了1个新的时滞相关稳定判据,使文中的时滞不确定随机系统是鲁棒均方指数稳定的.给出了具体的数值例子说明了研究结果的可行性和有效性.     

时滞广义时变系统的渐近稳定与镇定

研究了时滞广义时变系统的渐近稳定和镇定问题。首先利用相关不等式,通过建立Lyapunov方程,给出了1个时滞广义时变系统无脉冲、渐近稳定性的充分条件。然后,基于这一工作,利用Riccati方程,进一步研究了时滞广义时变系统的镇定问题。最后,举例说明该结论的可行性。     

多滞后中立型非线性控制系统的镇定

应用Lyapunov等价法讨论了多滞后中立型非线性定常控制系统与不带滞后的线性定常控制系统的镇定问题.应用Lyapunov稳定性理论与Krosovskii最大最小特征值定理,得到了多滞后中立型非线性定常控制系统渐近稳定的结论,该结论是对前人结果的进一步扩展,并在非线性项的限制下给出了时滞的界限.最后,将上述结论推广到了多滞后中立型非线性时变控制系统.     

线性关联滞后广义大系统的变结构控制

研究了一类线性关联滞后广义大系统的变结构控制综合问题.首先根据系统的结构和控制输入的特定形式,引入了1种新的受限系统等价分解形式,把每个子系统分解成2个低维的动态子系统：1个是不带控制项的线性关联微分差分系统,另1个是带有控制项的线性关联差分系统.然后设计了带有积分动态补偿器的切换函数, 给出了滑动模渐近稳定的充分条件.最后设计了可以保证系统的解的轨迹到达切换流形的多层分散变结构控制.这种控制对物理上分散等类型的线性关联滞后广义系统是合理的有效的.     

线性常时滞时变系统的有限时间稳定性分析

本文研究了一类线性常时滞时变系统的有限时间有界与输入-输出有限时间稳定性问题,通过构造Lyapunov泛函,并利用时变的矩阵不等式,分别获得了线性常时滞时变系统的有限时间有界和输入-输出有限时间稳定的充分条件。同时,设计了状态反馈控制器,使得闭环系统有限时间有界且输入-输出有限时间稳定,并通过仿真算例验证了本文方法的有效性。     

S分布时滞静态神经网络的全局渐近同步性

本文研究了一类S分布时滞静态神经网络模型作为驱动-响应系统的全局渐近同步性。在激活函数满足全局Lipschitz连续的条件下,设计了相应的响应系统的控制器,应用Lyapunov泛函方法及一些不等式技巧,得到了易于应用驱动—响应系统全局渐近同步性的的充分性判别准则。最后,通过实例验证了所得结论的有效性。     

具有小时滞的线性系统次优控制的无滞后转换法

该文研究线性时滞定常系统的次优控制问题。根据无滞后转换法的思想 ,先引入状态向量的增量 ,将其视为附加扰动输入 ,再利用微分方程的逐次逼近法 ,将既含有时滞项又含有超前项的两点边值问题化为既不含时滞项又不含超前项的两点边值问题族。然后 ,把第 N次逼近得到的控制律近似为系统的最优控制律 ,得到次优控制律。并用实例仿真验证了该算法的有效性。该方法可使小时滞系统的迭代次数大大减少 ,因此尤其适合于小时滞系统的次优控制。     

Large aperture digital acoustic array

A digital array of 120 acoustic channels 900 m in length has been constructed to study low-frequency (20-200 Hz) ambient noise in the ocean. The array may be deployed vertically or horizontally from the research platform FLIP and the array elements are localized with a high-frequency acoustic transponder network. The authors describe the instrumentation, telemetry, and navigation systems of the array during a vertical deployment in the northeast Pacific. Preliminary ambient noise spectra are presented for various array depths and local wind speeds. Ambient noise in the frequency band above 100 Hz or below 25 Hz increases with local wind speed. However, in the frequency band 25-100 Hz, ambient noise is independent of wind speed and may be dominated by shipping sources     

Fronts in Large Marine Ecosystems

Oceanic fronts shape marine ecosystems; therefore front mapping and characterization are among the most important aspects of physical oceanography. Here we report on the first global remote sensing survey of fronts in the Large Marine Ecosystems (LME). This survey is based on a unique frontal data archive assembled at the University of Rhode Island. Thermal fronts were automatically derived with the edge detection algorithm of (Cayula and Cornillon, 1992), (Cayula and Cornillon, 1995) and (Cayula and Cornillon, 1996) from 12 years of twice-daily, global, 9-km resolution satellite sea surface temperature (SST) fields to produce synoptic (nearly instantaneous) frontal maps, and to compute the long-term mean frequency of occurrence of SST fronts and their gradients. These synoptic and long-term maps were used to identify major quasi-stationary fronts and to derive provisional frontal distribution maps for all LMEs. Since SST fronts are typically collocated with fronts in other water properties such as salinity, density and chlorophyll, digital frontal paths from SST frontal maps can be used in studies of physical–biological correlations at fronts. Frontal patterns in several exemplary LMEs are described and compared, including those for: the East and West Bering Sea LMEs, Sea of Okhotsk LME, East China Sea LME, Yellow Sea LME, North Sea LME, East and West Greenland Shelf LMEs, Newfoundland–Labrador Shelf LME, Northeast and Southeast US Continental Shelf LMEs, Gulf of Mexico LME, and Patagonian Shelf LME. Seasonal evolution of frontal patterns in major upwelling zones reveals an order-of-magnitude growth of frontal scales from summer to winter. A classification of LMEs with regard to the origin and physics of their respective dominant fronts is presented. The proposed classification lends itself to comparative studies of frontal ecosystems.     

Rapid warming of Large Marine Ecosystems

The need to understand local effects of global climate change is most urgent in the Large Marine Ecosystems (LMEs) since marine ecosystem-based management requires information on the LME scale. Reported here is a study of sea surface temperature (SST) change in the World Ocean LMEs in 1957–2006 that revealed strong regional variations in the rate of SST change. The rapid warming in 1982–2006 was confined to the Subarctic Gyre, European Seas, and East Asian Seas. These LMEs warmed at rates 2–4 times the global mean rate. The most rapid warming was observed in the land-locked or semi-enclosed European and East Asian Seas (Baltic Sea, North Sea, Black Sea, Japan Sea/East Sea, and East China Sea) and also over the Newfoundland–Labrador Shelf. The Indian Ocean LMEs’ warming was slow, while two major upwelling areas – California and Humboldt Currents – experienced a slight cooling. The Subarctic Gyre warming was likely caused by natural variability related to the North Atlantic Oscillation. The extremely rapid surface warming in the enclosed and semi-enclosed European and East Asian Seas surrounded by major industrial/population agglomerations may have resulted from the observed terrestrial warming directly affecting the adjacent coastal seas. Regions of freshwater influence in the European and East Asian Seas seem to play a special role in modulating and exacerbating global warming effects on the regional scale.     

古代的巨大滑坡

在将近 70～ 60 Ma前的白垩纪末 ,地球与巨大的小行星或慧星相撞 ,释放出相当于里氏1 2～ 1 3级地震的能量。已确定有巨大的碎石降落在了墨西哥湾南部边缘 ,并引起海啸。乌兹霍尔海洋研究所的美国地质学家 R DNorris等研究发现 ,降落的巨石导致北美东部大部分地区——其大陆边缘和大西洋陆坡发生了大规模的滑坡。这一事件的痕迹保留在古时的强大海流沉积层中 ,这已经通过对取自大陆边缘百慕大群岛和格兰德浅滩之间的两个柱状沉积物样的研究得以证实。古代的巨大滑坡@朱佛宏     

Large eddy simulation of breaking waves

A numerical model is used to simulate wave breaking, the large scale water motions and turbulence induced by the breaking process. The model consists of a free surface model using the surface markers method combined with a three-dimensional model that solves the flow equations. The turbulence is described by large eddy simulation where the larger turbulent features are simulated by solving the flow equations, and the small scale turbulence that is not resolved by the flow model is represented by a sub-grid model. A simple Smagorinsky sub-grid model has been used for the present simulations. The incoming waves are specified by a flux boundary condition. The waves are approaching in the shore-normal direction and are breaking on a plane, constant slope beach. The first few wave periods are simulated by a two-dimensional model in the vertical plane normal to the beach line. The model describes the steepening and the overturning of the wave. At a given instant, the model domain is extended to three dimensions, and the two-dimensional flow field develops spontaneously three-dimensional flow features with turbulent eddies. After a few wave periods, stationary (periodic) conditions are achieved. The surface is still specified to be uniform in the transverse (alongshore) direction, and it is only the flow field that is three-dimensional.The turbulent structures are investigated under different breaker types, spilling, weak plungers and strong plungers. The model is able to reproduce complicated flow phenomena such as obliquely descending eddies. The turbulent kinetic energy is found by averaging over the transverse direction. In spilling breakers, the turbulence is generated in a series of eddies in the shear layer under the surface roller. After the passage of the roller the turbulence spreads downwards. In the strong plunging breaker, the turbulence originates to a large degree from the topologically generated vorticity. The turbulence generated at the plunge point is almost immediately distributed over the entire water depth by large organised vortices. Away from the bed, the length scale of the turbulence (the characteristic size of the eddies resolved by the model) is similar in the horizontal and the vertical direction. It is found to be of the order one half of the water depth.     

Large phillipsite crystal as ferromanganese nodule nucleus

We report here the occurrence of, to date, the largest (21 × 10 × 8 mm) phillipsite crystal forming the nucleus of a diagenetically formed ferromanganese nodule from the Central Indian Ocean Basin (CIOB). Assuming an average rate of ferromanganese nodule accretion as ~ 2 mm/Ma and that of phillipsite growth as ~ 0.65 mm/Ka, the nucleus material appears to have been growing for ~4.5–5 Ma. Originally surfaced as a rock fragment from late Miocene volcanism, this nucleus was later altered to phillipsite under alkaline, silica-undersaturated, low-temperature conditions through the length of the Neogene sedimentary hiatus.     

Large angular motions of tethered surface buoys

A three-dimensional coupled analysis of the interaction of a floating buoy and its mooring is studied. External loads include hydrodynamic forces, tether tensions, wind loads and system weight and buoyancy. Nonlinearities include large rotational and translational motions and non-conservative fluid loads. The mooring problem is formulated as a nonlinear two-point-boundary-value-problem. At each instant in time, the mooring problem is solved by direct integration using a successive iterative algorithm to satisfy boundary conditions. Buoy kinetic and kinematic equations are derived assuming large angles represented by Euler parameters. Coupling between the buoy and the mooring is enforced by matching the velocities of the tether and buoy at the attachment point. A predictor-corrector coupling algorithm is used with multiple sizes of time steps used to provide stability for the separate mooring and buoy models. Numerical results are compared to experimental responses of three types of buoys (sphere, spar and disc) subject to both regular and irregular waves.     

一种基于GPU的大规模地形实时生成算法

大规模地形实时可视化一直以来都是计算机图形学、虚拟现实和仿真领域研究的重点和热点。利用Geometry Clipmap算法的基本思想,改进了数据的组织方法,简化了算法的裂缝消除技术,对视景体的裁切算法进行了改进,实现了海量数据的实时可视化。     

大型AUV及其水面侦察技术浅析

传统的自主水下无人航行器（AUV）主要执行包括军事活动在内的水下情报收集、环境监测和水下目标探测与处置等。近年来随着信息化技术和人工智能的发展,AUV行业受到各界尤其是各国军方越来越多的关注,得到了快速发展和广泛应用。作为一种无人侦察平台,AUV逐渐突破了常规尺度,向大型化和超大型化方向发展,可搭载的载荷类型和尺度有了明显的变化和提升。通过分析大型AUV作为侦察型装备的国内外发展现状,对利用大型AUV开展水面侦察的能力建设进行了分析,重点提出了大型AUV搭载水面侦察载荷需要解决的关键技术,为进一步提升和拓展AUV作战能力和作战领域提供支持。     

Large eddy simulation of spilling and plunging breakers

A Navier–Stokes solver with a free surface model is used for simulating wave breaking, undertow, and turbulence in breaking waves. The free surface model is based on the Volume of Fluid concept. Turbulence scales larger than the grid scale are simulated directly while turbulence scales smaller than the grid scale are represented by a sub-grid scale model. Two different approaches for the sub-grid scale model have been applied, which are the Smagorinsky model and a model based on a k-equation for the sub-grid scale turbulence. The waves approach the shore in shore-normal direction and break on a plane constant sloping beach. Periodic spilling and plunging breakers are simulated for 20 and 16 wave periods, respectively. The set-up, undertow, and turbulence levels are compared to experimental results. Despite the rather coarse resolution of the computational domain, satisfactory results for the wave height decay and undertow have been obtained. However, the turbulence levels are over-predicted when using the standard values of the model parameters and a complete answer to this problem has not been found. Furthermore, the evolution of vorticity over the wave period has been studied. It shows that at the initial breaking point vorticity is generated around the vertical as well as around the transverse axis. Later vorticity around the longitudinal axis (offshore–onshore direction) is generated, probably through deformation of vorticity around the other axis.