標(biāo)題: Titlebook: Dynamics of the West Antarctic Ice Sheet; Proceedings of a Wor C. J. Veen,J. Oerlemans Conference proceedings 1987 D. Reidel Publishing Com [打印本頁(yè)] 作者: intrinsic 時(shí)間: 2025-3-21 16:29
書目名稱Dynamics of the West Antarctic Ice Sheet影響因子(影響力)
書目名稱Dynamics of the West Antarctic Ice Sheet影響因子(影響力)學(xué)科排名
書目名稱Dynamics of the West Antarctic Ice Sheet網(wǎng)絡(luò)公開度
書目名稱Dynamics of the West Antarctic Ice Sheet網(wǎng)絡(luò)公開度學(xué)科排名
書目名稱Dynamics of the West Antarctic Ice Sheet被引頻次
書目名稱Dynamics of the West Antarctic Ice Sheet被引頻次學(xué)科排名
書目名稱Dynamics of the West Antarctic Ice Sheet年度引用
書目名稱Dynamics of the West Antarctic Ice Sheet年度引用學(xué)科排名
書目名稱Dynamics of the West Antarctic Ice Sheet讀者反饋
書目名稱Dynamics of the West Antarctic Ice Sheet讀者反饋學(xué)科排名
作者: 紀(jì)念 時(shí)間: 2025-3-21 20:24
Quantitative Estimates of the Mass Flux and Ice Movement Along the Ice Edges in the Eastern and Sour than previous estimates..Most of the major ice shelves in the Weddell Sea region show steadily advancing ice fronts during the period of observation. This has the consequence that the source region for icebergs during this time should be limited mainly to ice fronts in the eastern Weddell Sea. The作者: 損壞 時(shí)間: 2025-3-22 02:43 作者: lesion 時(shí)間: 2025-3-22 08:28 作者: 未開化 時(shí)間: 2025-3-22 09:18
Ice Stream-Ice Shelf Interaction in West Antarctica,d ridges instead of the smoother surface of Ice Stream C. Regions of Ice Stream B with a lower surface elevation move faster than higher elevation regions, presumably because the lower-elevation ice is thinner and experiences less basal friction. Surface strain rates at Ice Stream B vary on a scale 作者: 里程碑 時(shí)間: 2025-3-22 15:28
Longitudinal Stresses and Basal Sliding: A Comparative Study,975). In the latter model, longitudinal deviatoric stresses play a minor role and have very little effect on the model results. The two other models yield virtually the same results. This means that indeed the gradient of the deviatoric stress along a flowline may be neglected. In fact, the results 作者: 里程碑 時(shí)間: 2025-3-22 17:17
A Subglacial Aquifer Bed Model and Water Pressure Dependent Basal Sliding Relationship for a West Aund to be the cause of the 1982–1983 surge of Variegated Glacier in Alaska, may be typical of the flow regime of this ice stream. The bed model and inferred subglacial water pressures are consistent with (1) the calculated subglacial water flux, (2) the thickness of a porous water-saturated subglaci作者: 追逐 時(shí)間: 2025-3-23 00:58
Numerical Modelling of the Large-Scale Basal Water Flux under the West Antarctic Ice Sheet, pattern of steady-state mean water-film thickness is then interpreted in terms of its possible relationships to the basal sliding rates and the basal shear stress particularly under the major ice streams.作者: 兒童 時(shí)間: 2025-3-23 02:48
Modelling the Response of the West Antarctic Ice Sheet to a Climatic Warming, the Antarctic ice shelves and the resulting increased strain rates which could then occur near the grounding lines..A hierarchy of ice-sheet modelling studies has been carried out covering the fast-flowing ice streams, the ice sheet thermal regime and the whole Antarctic at a coarser resolution. Th作者: Metamorphosis 時(shí)間: 2025-3-23 09:15
Women Entrepreneurs and Successr than previous estimates..Most of the major ice shelves in the Weddell Sea region show steadily advancing ice fronts during the period of observation. This has the consequence that the source region for icebergs during this time should be limited mainly to ice fronts in the eastern Weddell Sea. The作者: 調(diào)色板 時(shí)間: 2025-3-23 09:50
Clinton Jeffery,Jafar Al-Gharaibehcan be fitted reasonably well by making a number of simplifying assumptions. In addition, velocities are known at the grounding line of the Rutford Ice Stream and across the ice rumples between Korff and Henry ice rises. Velocity profiles can be deduced along the two relevant flowlines using the pri作者: Working-Memory 時(shí)間: 2025-3-23 15:05
Evaluating Complex Development Programsure evolution of the Ross Ice Shelf, and of the stress regime at the grounding line of ice streams B and C are simulated to assess the response to impulsive removal of the Crary Ice Rise. This simulation shows that the forces restraining Ice Stream B do not change by a significant amount even after 作者: monochromatic 時(shí)間: 2025-3-23 20:43
https://doi.org/10.1007/978-1-4614-4797-9d ridges instead of the smoother surface of Ice Stream C. Regions of Ice Stream B with a lower surface elevation move faster than higher elevation regions, presumably because the lower-elevation ice is thinner and experiences less basal friction. Surface strain rates at Ice Stream B vary on a scale 作者: 惹人反感 時(shí)間: 2025-3-23 23:52 作者: Affirm 時(shí)間: 2025-3-24 03:06
https://doi.org/10.1007/978-1-4614-9123-1und to be the cause of the 1982–1983 surge of Variegated Glacier in Alaska, may be typical of the flow regime of this ice stream. The bed model and inferred subglacial water pressures are consistent with (1) the calculated subglacial water flux, (2) the thickness of a porous water-saturated subglaci作者: 溫順 時(shí)間: 2025-3-24 10:26
Daniel B. Cornfield,Randy Hodson pattern of steady-state mean water-film thickness is then interpreted in terms of its possible relationships to the basal sliding rates and the basal shear stress particularly under the major ice streams.作者: 植物群 時(shí)間: 2025-3-24 10:42 作者: FRET 時(shí)間: 2025-3-24 15:24
0924-5006 centimeters (e. g. thermal expansion, change in mass balance of glaciers and ice sheets). But the picture of the carbon dioxide problem has frequently be made m978-94-010-8171-9978-94-009-3745-1Series ISSN 0924-5006 作者: Conserve 時(shí)間: 2025-3-24 21:04 作者: 不成比例 時(shí)間: 2025-3-25 02:58 作者: 中國(guó)紀(jì)念碑 時(shí)間: 2025-3-25 03:57 作者: dagger 時(shí)間: 2025-3-25 10:35 作者: addict 時(shí)間: 2025-3-25 15:07 作者: Incorruptible 時(shí)間: 2025-3-25 17:53
Women’s Approach to Economics and Firmsnts in it cause glacial motion as described by the driving stress. The remaining stresses oppose the motion and in assessing glacial stability it is important to determine which of the several potential resistive forces are most important, Data relating to the stresses driving and resisting the flow作者: conceal 時(shí)間: 2025-3-25 20:18 作者: 加強(qiáng)防衛(wèi) 時(shí)間: 2025-3-26 03:22
Women Entrepreneurs and Success apparent ice movements for the period under consideration, i.e. apparent advance rates and azimuths of ice-edge alteration during particular time intervals. The near-ice-edge movements thus determined are in good agreement with the ice movement as derived from interpretation of Landsat images and W作者: 凹槽 時(shí)間: 2025-3-26 08:06
Clinton Jeffery,Jafar Al-Gharaibehic Survey since 1975. Comprehensive cover was obtained during the 1982/83 season with flight lines at approximately 50 km spacing. The major features described previously are confirmed, but additional information over the western half of the ice shelf where there were few data before, has revealed t作者: 分解 時(shí)間: 2025-3-26 09:50 作者: 載貨清單 時(shí)間: 2025-3-26 16:08 作者: Brochure 時(shí)間: 2025-3-26 19:21
Evaluating Complex Development Programspredict the stress regime at an ice-stream grounding line when the ice-shelf flow geometry differs from ideal, rectangular channel flow. This inadequacy results from the action of glaciostatic stresses distributed around the margins of an ice shelf, which lead to a reaction force, termed ., at the g作者: DEMUR 時(shí)間: 2025-3-26 21:09 作者: 合乎習(xí)俗 時(shí)間: 2025-3-27 02:11
Amy Neustein,Judith A. Markowitze grounding line. The transition flow is found numerically by solving a non-linear elliptic differential equation with fixed boundary conditions. The transition zone is located around the grounding line and its width is of the order of the ice thickness. In the case of basal sliding the transition z作者: Aspiration 時(shí)間: 2025-3-27 07:37 作者: Mobile 時(shí)間: 2025-3-27 11:46 作者: Flounder 時(shí)間: 2025-3-27 17:02
https://doi.org/10.1007/978-1-4614-9123-1ge is 3 to 18 m./s at the grounding line. The inferred subglacial water pressure is greater than 90 % of the ice overburden pressure for the entire 300 km length of the ice stream, and greater than 96 % of the ice overburden pressure for 230 km upglacier from the grounding line. This suggests that t作者: CAND 時(shí)間: 2025-3-27 21:17 作者: caldron 時(shí)間: 2025-3-28 01:52 作者: 集合 時(shí)間: 2025-3-28 03:18
https://doi.org/10.1007/978-1-4615-0659-1 change. One of the most severe consequences alluded to is the possibility of a rapid rise in sea level resulting primarily from increased melting of the Antarctic Ice Sheet — particularly from West Antarctica where much of the ice is currently grounded well below sea level..The present generation o作者: Distribution 時(shí)間: 2025-3-28 08:21
Dynamics of the West Antarctic Ice Sheet978-94-009-3745-1Series ISSN 0924-5006 作者: Flatter 時(shí)間: 2025-3-28 12:29
Women’s Entrepreneurship and Economics water reservoir). Nevertheless, small changes in ice volume can have large effects on sea level. For instance, a 1% change in ice volume results in a sea-level rise or drop of some 70 cm. So although the large ice caps are located in remote areas of the world, their evolution leaves a clear mark upon the regions in which we live.作者: 嚴(yán)厲譴責(zé) 時(shí)間: 2025-3-28 18:35
Amy Neustein,Judith A. Markowitze grounding line. The transition flow is found numerically by solving a non-linear elliptic differential equation with fixed boundary conditions. The transition zone is located around the grounding line and its width is of the order of the ice thickness. In the case of basal sliding the transition zone can be widened considerably.作者: 變白 時(shí)間: 2025-3-28 20:18 作者: 圣歌 時(shí)間: 2025-3-29 00:41
https://doi.org/10.1007/978-94-009-3745-1Ice shelf; Scale; atmosphere; climate; subglacial; temperature; water; hydrogeology作者: blithe 時(shí)間: 2025-3-29 05:43 作者: 怪物 時(shí)間: 2025-3-29 07:52
Evaluating Complex Development ProgramsWe report here on some of the results of our first two seasons work along the Siple Coast. These results are all preliminary in nature and could be modified substantially with further analysis. Furthermore, we have selected from a much larger body of data only a few points that we believe will be of interest to this workshop.作者: Collar 時(shí)間: 2025-3-29 13:17
A Few Preliminary Results from the Glaciogeophysical Survey of the Interior Ross Embayment (GSIRE),We report here on some of the results of our first two seasons work along the Siple Coast. These results are all preliminary in nature and could be modified substantially with further analysis. Furthermore, we have selected from a much larger body of data only a few points that we believe will be of interest to this workshop.作者: Expediency 時(shí)間: 2025-3-29 17:40
The West Antarctic Ice Sheet: The Need to Understand Its Dynamics, water reservoir). Nevertheless, small changes in ice volume can have large effects on sea level. For instance, a 1% change in ice volume results in a sea-level rise or drop of some 70 cm. So although the large ice caps are located in remote areas of the world, their evolution leaves a clear mark up作者: Digest 時(shí)間: 2025-3-29 22:30 作者: 同步信息 時(shí)間: 2025-3-30 02:07 作者: 閑蕩 時(shí)間: 2025-3-30 04:59
Quantitative Estimates of the Mass Flux and Ice Movement Along the Ice Edges in the Eastern and Sou apparent ice movements for the period under consideration, i.e. apparent advance rates and azimuths of ice-edge alteration during particular time intervals. The near-ice-edge movements thus determined are in good agreement with the ice movement as derived from interpretation of Landsat images and W作者: 前面 時(shí)間: 2025-3-30 12:16 作者: Affable 時(shí)間: 2025-3-30 14:34
Unconfined Ice-Shelf Flow,ss in both directions. Exploiting the slow variation of physical quantities in both horizontal directions compared to vertical variation allows simple solution of the vertical momentum balance and the derivation of plane stress equilibrium equations for integrals of the horizontal stresses through t作者: 正常 時(shí)間: 2025-3-30 19:56 作者: 小步舞 時(shí)間: 2025-3-30 23:40
Ice-Shelf Backpressure: Form Drag Versus Dynamic Drag,predict the stress regime at an ice-stream grounding line when the ice-shelf flow geometry differs from ideal, rectangular channel flow. This inadequacy results from the action of glaciostatic stresses distributed around the margins of an ice shelf, which lead to a reaction force, termed ., at the g作者: 含糊其辭 時(shí)間: 2025-3-31 01:41
Ice Stream-Ice Shelf Interaction in West Antarctica, of base camps which were established in the mouths of ice streams B and C and at the upstream edge of Crary Ice Rise. The annual rate of ice deformation in Ice Stream C is very small, generally less than 10. yr.. Reoccupation of an 11 year old stake network permitted ice motion (6.1 m/yr) and groun作者: 毗鄰 時(shí)間: 2025-3-31 06:49 作者: 鍵琴 時(shí)間: 2025-3-31 11:29 作者: Exclaim 時(shí)間: 2025-3-31 16:10 作者: endocardium 時(shí)間: 2025-3-31 18:09
A Subglacial Aquifer Bed Model and Water Pressure Dependent Basal Sliding Relationship for a West Age is 3 to 18 m./s at the grounding line. The inferred subglacial water pressure is greater than 90 % of the ice overburden pressure for the entire 300 km length of the ice stream, and greater than 96 % of the ice overburden pressure for 230 km upglacier from the grounding line. This suggests that t作者: 影響 時(shí)間: 2025-3-31 22:47
The Heat Budget of the Ross Drainage Basin,s from the fact that dissipative heating can be calculated directly from the release of gravitational energy. When mass balance, surface temperature and geothermal input are known, the mean ice temperature at the grounding line can be obtained as a residual..The procedure is applied to the drainage 作者: voluble 時(shí)間: 2025-4-1 01:56
Numerical Modelling of the Large-Scale Basal Water Flux under the West Antarctic Ice Sheet,eratures and melt rates for a wide range of values of the geothermal flux. Steady state is assumed and ice “balance velocities” are computed from continuity and used in the heat-conduction equation. As the geothermal flux increases, the melt area increases and becomes connected to the water under th作者: Anthrp 時(shí)間: 2025-4-1 07:01 作者: 眉毛 時(shí)間: 2025-4-1 11:10
