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Perilous Promises by Jean Rossetta Download PDF EPUB FB2
However Christi Williams' Perilous Promises was a book I made an exception for. Perilous Promises is the story of a woman named Perris's journey after breast cancer, who she wants to be, and the painful, but necessary decision to divorce her loving but suffocating husband (and love of her life), Noah/5.
However Christi Williams' Perilous Promises was a book I made an exception for. Perilous Promises is the story of a woman named Perris's journey after breast cancer, who she wants to be, and the painful, but necessary decision to divorce her loving but suffocating husband (and love of her life), Noah/5(12).
Perilous Promises [Rossetta, Jean] on *FREE* shipping on qualifying offers. Perilous Promises4/5(3). A Perilous Promise book. Read 15 reviews from the world's largest community for readers.
“The author draws as much from Fawlty Towers as she does from Ag /5. COVID Resources. Reliable information about the coronavirus (COVID) is available from the World Health Organization (current situation, international travel).Numerous and frequently-updated resource results are available from this ’s WebJunction has pulled together information and resources to assist library staff as they consider how to handle.
The characters and events portrayed in this book are fictitious. Any similarity to real persons, living or dead, is coincidental and not intended by the author.
Summary: Reynie, Kate, Sticky, and Constance, all graduates of the Learning Institute for the Very Enlightened and members of the Benedict Society, embark on a scavenger hunt that turns. The Paperback of the Perilous Promises by Jean Rossetta at Barnes & Noble.
FREE Shipping on $35 or more. Due to COVID, orders may be delayed. Thank you for your patience. Book Annex Membership Educators Gift Cards Stores & Events Help Auto Suggestions are available once you type at least 3 letters. Publish your book with B&: Jean Rossetta. Altercation is the sequel to Perilous.
“These books are riveting. I couldn’t put either of them down once I’d started, and this is a series where the sequel is even better than the first book.” (Shannon O’Donnell, Book Dreaming) The FBI promises Jacinta Rivera and her friends that they are safe. [ Read Book ] Perilous Promises ☣ MOBI eBook or Kindle ePUB free.
Posted on 07 November 29 April By Christi Williams. This dark and compelling world is filled with enticing romance as well as perilous adventure. The Black Dagger Brotherhood series promises tons of thrills and chills.”—RT Book Reviews “You will lose yourself in this world; it is different, creative, dark.
A Perilous Promise (Pennyfoot Hotel Mystery Book 0) eBook: Kate Kingsbury: : Kindle Store/5(19). Whatever your problems, whatever your needs, the answers are in the Bible. This remarkable book includes more than 1, promises from Scripturepromises you can count on.
The verses are arranged alphabetically by more than 60 topics for quick and easy reference. pages, softcover from Barbour. The Bible Promise Book, KJV ()/5().
Sensational Nightingales - Every Promise In The Book Is Mine 40 prayers to cleanse our hearts. 40 prayers to seek direction when we have lost our way.
40 prayers to help us turn back to You. 40 prayers to heed Your warnings for You are a just God. 40 prayers for Your glory to fill our churches and homes mightily, so all the world will see and know that You, alone, are God.
Do not withhold your mercy from. I am constantly surprised at where Jack Campbell can take these books and especially love that Perilous Shield had so much space action. The one thing that kept this from being a 5 star book for me was the ending (a cliffhanger for the next book in the series) which ended up playing out too much like an overwrought Mexican Telenovela soap opera.
Sponsor azu/promises-book Watch 44 Star k Fork Code. Issues Pull requests 0. Actions Projects 0. Security Insights Dismiss Join GitHub today. GitHub is home to over 40 million developers working together to host and review code, manage projects, and build software together.
Buy a cheap copy of A Perilous Proposal book by Michael R. Phillips. Two years have passed since the conclusion of the Shenandoah Sisters series, and Katie and Mayme are young women with big dreams, running Rosewood with the help of Free shipping over $/5(5).
Bride of the Castle - Ebook written by John DeChancie. Read this book using Google Play Books app on your PC, android, iOS devices.
Download for offline reading, highlight, bookmark or take notes while you read Bride of the Castle/5(2). A Promised Land: A Perilous Journey: Theological Perspectives on Migration is a compilation of essays that brings together Christian leaders and lay people, cultural anthropologists and sociologists, practioners and professors, Scalabrinian missionaries, and theologians on the theme of the U.S.-Mexico border and migration.
Faithful Living in Perilous Times “For I am not ashamed of the gospel of Christ, for it is the power of God for salvation for everyone who believes, for the Jew first and also for the Greek.
For in it the righteousness of God is revealed from faith to faith; as it is written, ‘The just shall live by faith.’” Romans – Art & Science of Teaching / The Perils and Promises of Discovery Learning. Robert J. Marzano. Unassisted discovery learning is perilous to student learning, but enhanced discovery learning can be a useful instructional tool.
In K–12 education, it's almost a cliché to say that discovery learning is superior to learning derived from direct. Perilous Times: Free Speech in Wartime: From the Sedition Act of to the War on Terrorism by Geoffrey R. Stone in EPUB, RTF, TXT download e-book.
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The conclusion sets up what promises to be many adventures to come. Wondering if A Dastardly Plot: A Perilous Journey of Danger & Mayhem, Book 1 is OK for your kid. Set preferences and get age-appropriate recommendations with Common Sense Media Plus.4/5.
While the language used in the Book of Revelation may make you fearful, that's not the intent. There is no need to fear with Jesus. Here are seven end time promises that will give you hope.
Some promises can, perhaps, be broken but not the promises of love. when she takes that courageous chance, it is the most perilous choice of all. Praise for the novels of Katherine Stone: Katherine Stone writes in the vein of Danielle Steel and Sandra Brown.
- Library Journal Midwest Book Review on Bed of Roses Remarkably romantic Brand: ChaseStone. See also Second Coming of Jesus Christ; Signs of the Times. The time in which we now live. The days (or dispensation of time) just before the Second Coming of the Lord. I tell you what shall befall you in the last days, Gen.
The Redeemer shall stand at the latter day upon the earth, Job In the last days, the Lord’s house shall be established, Isa. The Scripture says perilous times will come, but believers are not to be troubled by them.
Author and pastor Happy Caldwell reveals how to live in victory regardless of circumstances - by knowing God's promises of provision and protection and releasing your faith to : Ebook. Eileen T. Flaherty is a longtime legal and compliance professional who is currently managing director of The Global Capital Group Ltd., a legal and regulatory consulting firm.
She is. Find helpful customer reviews and review ratings for A Perilous Promise (Pennyfoot Hotel Mystery Book 0) at Read honest and unbiased product reviews from our users/5. Sarah Kessler, the deputy editor for Quartz at Work and a former reporter for Fast Company, took an in-depth look at what it means to live as a gig worker in her new book Gigged: The End of the.
40 Prayers for Perilous Times – Day A person standing alone can be attacked and defeated, but two can stand back-to-back and conquer. Three are even better, for a triple-braided cord is not easily broken.
Ecclesiastes Swimming upstream. That’s what it feels like, Lord. I struggle to keep a forward momentum, a rush of icy water.Perilous Times By John Owen () "This know also, that in the last days perilous times shall come." 2 Timothy The words contain a warning of imminent dangers.
And there are four things in them: First, the manner of the warning: "This know also," Secondly, the evil itself that they are warned of: "Perilous times.".


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Flying South Cholla Stairs create an awesome way for your bird to climb around their birdcage. The stairs provide your feathered friend with a bird toy and a bird perch. The perches are approximately 4 inches in length. They can be placed in different positions to help your bird climb from the bottom of its cage to its favorite perch. These awesome Flying South perches are perfect for all sizes of birds.
3 Cholla Stairs Perches are Included!
All Teddy Bear Cholla Perches vary in length, diameter, and style.
3-4" in length
2 1/4 x 2 1/2" in diameter

domain: pet


Newly appointed to Illinois Governor JB Pritzker’s capital infrastructure committee Marc Poulos says promises made by former transportation secretary regarding I-80 are expected to come to fruition. Those include, minutemen and cantilever signs.
At WJOL’s RUSH meeting a year ago, then transportation secretary Randy Blankenhorn made those promises to Residents United For Safer Highways as way to mitigate the dangers of I-80 with the influx of trucks and population growth in Will County. Poulos attended the RUSH meetings and in his new position expects I-80 to be part of a new capital improvement bill this spring.
Poulos says everything is on the table including turning I-80 into a tollway and says Governor Pritzker realizes the importance of the I-80 corridor.
To hear the entire interview click below.


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Including Lichens, Liverworts, and Other MiniaturesBook - 1997
A delightful book that encourages gardeners to pay closer attention to the subtle beauty of miniature landscapes and introduces one of the glories of Japanese gardens into American designs. The author writes entertainingly of mosses on rocks and walls, in containers, and as a lush ground cover, and he presents a gallery of his favorite moss species.
Publisher: Portland, Or. : Timber Press, c1997
Branch Call Number: 635.9 SCH
Characteristics: 261 p. :,col. ill. ;,24 cm

domain: library


The gradual evolution of the automobile has meant that different innovations have arrived at different times, and leaping back 90 years in automotive history makes for a strange combination of the familiar and the utterly alien. It’s a point made spectacularly well by the Bentley Blower Continuation, a vehicle that manages the unique trick of possessing both a new-car smell and a genuine pre-war driving experience.
The Blower’s dial-strewn dashboard seems to have been modeled on the mantelpiece of an English country manor, yet it houses both a tachometer and a speedometer—features that few cars had in 1930. It doesn’t have a fuel gauge, however. A period Blower’s owner—or, likely, their servant—would have checked the car’s fuel level by simply gazing into its vast, 26.4-gallon tank. The Blower’s floor-mounted gearshift is laid out in a conventional H pattern—top left for first gear, bottom right for fourth—although it is positioned awkwardly to the right of the right-hand driving position. The clutch pedal also is where your left foot expects to find it. But things get more archaic with the realization that this vintage of Bentley predates conventionally modern pedal positioning, what with its accelerator situated in the middle and the brake pedal on the right.
In short, Bentley has done what it promised when it announced it would build a run of 12 of its most famous cars. Beyond the lack of 90 years of wear, the Continuation is an exact facsimile of the original Blower. Jaguar kicked off the modern trend for factory-sanctioned continuation models in 2015 by producing seven lightweight E-types that the company had originally planned but never got around to making. Additional models have followed. Aston Martin also got in on the act with old-new versions of the DB4 GT, DB4 GT Zagato, and the James Bond-inspired DB5 Goldfinger.
But when Bentley’s Mulliner division decided to do something similar, it opted to head much further back in time and to deliver what is a much more demanding driving experience. Yet, there was no shortage of interest. The company says it could have sold considerably more than the dozen cars it will build, despite each example costing $2.1 million and not being suitable for registered road use in most parts of the world.
Despite being one of Bentley’s most famous models, the original Blower wasn’t a factory project. Company founder W.O. Bentley didn’t believe in forced induction, holding that larger naturally aspirated engines were a more appropriately English way to respond to the challenge posed by rival supercharged racers such as the Mercedes SSK and Bugatti Type 35C. One-time fighter pilot and aristocratic Bentley Boy driver, Sir Henry “Tim” Birkin, politely disagreed and set about building a four-cylinder car that would use an Amherst-Villiers Roots-type supercharger to produce more power than the Bentley Works team’s Speed Sixes. Doing this cost Birkin most of his personal fortune, and when that ran short, he managed to arrange additional support from a wealthy heiress named Dorothy Paget, a prolific gambler and racehorse owner. Eventually he persuaded Woolf Barnato, Bentley’s chairman and another factory race driver, to sanction the production of 55 Blowers, five of which would be outfitted for racing.
Featuring such innovations as a 16-valve cylinder head, twin-spark ignition, aluminium pistons, and a magnesium crankcase, the Blower’s 4.4-liter four was one of the most powerful in the world at that time, making 240 horsepower in race trim. That was more than the 200 or so horses made by the massive Speed Six cars—the ones that Ettore Bugatti once referred to as the world’s fastest trucks. But the Blower was also thirsty and prone to failure. “The Blower eats plugs like a donkey eats hay,” as Bentley’s chief mechanic put it.
Some more history: The Bentley Blower never won a significant race in its day, although it did play a heroic cameo at the 1930 24 Hours of Le Mans. Bentley had won the endurance race in 1929 and was defending its title with three factory-entered Speed Sixes. Birkin brought another trio of Blowers, driving the No. 2 car himself. The big threat was Rudolf Caracciola’s privately entered Mercedes SSK, a car with a clear performance advantage over the Speed Six but considered mechanically fragile when driven flat-out. When the race began, Birkin set off at a searing pace, overtaking the Mercedes twice and goading the German into giving chase. Caracciola did, and his SSK indeed broke before the finish, but none of the Blowers made it to the checkered flag, either. Barnato in his Speed Six ultimately led a one-two finish for the works team.
Bentley now owns Birkin’s No. 2 car and reckons it is worth tens of millions of dollars. There have been various mild restorations over the years, but the core structure and engine are the same that raced in 1930. That car served as the basis for the Continuation project, with Mulliner disassembling it and scanning individual parts before commissioning exact replicas. The car in our photos is the development prototype, officially known as Car Zero, and it carries some extra paraphernalia required as a Volkswagen Group test mule, including both supplementary LED headlights and a data-acquisition system. But mechanically it is identical to both the original car and the dozen production models that will follow it.
Despite being worth far more than the Continuation, the No. 2 car is surprisingly the one Bentley asked us to sample first at Millbrook Proving Ground. This was to impart an appreciation for the car’s rich history and, as Bentley’s public-relations manager admits, because the teeth of its non-synchronized transmission have been smoothed by decades of graunchy gear changes and should therefore be slightly more forgiving in inexperienced hands.
Coping with the Blower’s gearbox is the greatest challenge when behind the wheel. The accurately named “crash” transmission requires double declutching—pressing the clutch pedal to deselect a gear, releasing it, and pressing it again to select a gear—for shifting both up and down its ratios, with downshifts bringing the additional complication of matching the engine’s revs to road speeds. The clutch also incorporates an engine brake to still the big four’s input shaft so that first gear can be selected. On the move, this means that downshifts bring the additional challenge of remembering to only depress the clutch halfway while blipping a wrongly placed accelerator and manipulating a shifter that’s partially positioned under your right thigh. Yes, there were some grinding noises.
But the rest of the experience of the No. 2 car feels, if not exactly modern, certainly less old-fashioned. Performance is impressively brisk. The big engine has no enthusiasm for revs and is reluctant to reach its modest 4500-rpm redline. But low-end torque is plentiful, and the boost gauge indicates the supercharger’s significant contribution even at low revs. When the original Blower team cars were sold off in 1931, Birkin guaranteed that each was able to achieve a top speed of at least 125 mph. We were restricted to an indicated 80 mph on Millbrook’s banked two-mile oval, but the Blower feels completely happy at this pace, tracking straight and with less slop in its steering than many later cars. Driving it is a physical experience. The steering barely lightens as the car gains speed, and the cable-operated drum brakes are feeble. Even panic-level pressures produce less retardation than resting your foot on the brake pedal of a modern vacuum-boosted braking system.
Switching to Car Zero confirms a nearly identical driving experience. The new car’s fresh gearbox is less tolerant of fluffed shifts, although the heavy shift mechanism feels more accurate. The prototype’s brakes are even worse—we later learned that it had been fitted with new pads that hadn’t been properly bedded—but we soon find that the sizeable external handbrake lever operates a separate set of shoes on the back axle, allowing rear braking force to be usefully increased. The engine emits the same thump-thump-thumpsoundtrack, and although it is limited to 3200 rpm during testing, the car actually feels slightly quicker than the original.
The greater difference is one of perception. The Continuation feels every bit as archaic to drive as its predecessor, but it’s not an irreplaceable historical artifact. We don’t mind pushing it harder on Millbrook’s Hill Route, which could pass for a narrow, twisty Alpine road. The combination of solid axles, leaf springs, and lever-arm dampers cope surprisingly well with harder cornering loads, although the ride feels brutally hard over even small bumps.
Peak cornering forces are modest, and the combination of narrow tires and the positively cambered front wheels make for limited grip and the early onset of understeer. Overall traction is decent, but the heavy, recirculating-ball steering tries to center itself when you call for more power with any steering lock applied. Within a couple of miles, it is clear that the biggest limitation to speed on a windy road is most likely to be the driver and their ability to wrestle the Blower through turns.
Bentley has done exactly what it needed to do with the Blower Continuation, and to have tamed or civilized it in any way would have entirely missed the point. Bentley’s first continuation model is also the most extreme of the genre so far. Here’s hoping it gives the upper echelons of the market an appetite for other equally impressive newly built anachronisms.
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Big-name games incoming
Whether we like it or not, we’ve already said goodbye to the hot days of Summer for the cooler days of Fall. Oddly enough, things are quite opposite for the Switch, as things will be heating up as we make our way through the next month.
As usual, another massive slate of big-name games is coming to the Switch, and Nintendo wants to make sure you’re up-to-date on what’s around the corner. October is looking like a month that’ll provide all sorts of gameplay experiences, with titles ranging from sports to simulation and everything in-between.
Wondering what some of October’s bigger Switch titles are? You can find Nintendo UK’s hand-picked recommendations here.


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Our 4 fabulous felines.
You may wonder how these four felines manage to get along so well in our home.
Most multi-cat households will have a 'top cat', and in our home, that would be Lily.
It seems that if all the cats understand this, things can run quite smoothly.
One of the ways of deciphering which cat is on the highest level in a home is to watch which one likes to be above the other cats any chance they get. One may take to the highest seat on the cat-tree or always sit on a wall-shelf looking down. Oddly, in our home I don't notice that happening at all. What I do notice is that at meal-time our Lily always eats first, especially if they are sharing some cut-up chicken on a large plate. Both Annie and Audrey wait until Lily has finished her portion before they dig in. I find that very interesting. Sometimes age will play a factor in status but an older, unhealthy cat can quickly lose the top cat position. That has not happened here as yet although our Lily is eighteen and has pancreatitis.
Sierra has always been an indoor-outdoor cat and has not included herself in the goings-on of our other three. She tends to eat by herself most times away from the others. I would say she is more of a loner.
Here is something to read on this subject if you are interested.
Even though I live with and work with cats, I realize that I will never really know 'the cat' completely. They will always be the most fascinating creatures to me and I learn something new about them every-day.


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A coupled sea ice–ocean model is developed to quantify the sea ice response to changes in atmospheric and oceanic forcing in the Bering Sea over the period 1970–2008. The model captures much of the observed spatiotemporal variability of sea ice and sea surface temperature (SST) and the basic features of the upper-ocean circulation in the Bering Sea. Model results suggest that tides affect the spatial redistribution of ice mass by up to 0.1 m or 15% in the central-eastern Bering Sea by modifying ice motion and deformation and ocean flows. The considerable interannual variability in the pattern and strength of winter northeasterly winds leads to southwestward ice mass advection during January–May, ranging from 0.9 × 1012 m3 in 1996 to 1.8 × 1012 m3 in 1976 and averaging 1.4 × 1012 m3, which is almost twice the January–May mean total ice volume in the Bering Sea. The large-scale southward ice mass advection is constrained by warm surface waters in the south that melt 1.5 × 1012 m3 of ice in mainly the ice-edge areas during January–May, with substantial interannual variability ranging from 0.94 × 1012 m3 in 1996 to 2.0 × 1012 m3 in 1976. Ice mass advection processes also enhance thermodynamic ice growth in the northern Bering Sea by increasing areas of open water and thin ice. Ice growth during January–May is 0.90 × 1012 m3 in 1996 and 2.1 × 1012 m3 in 1976, averaging 1.3 × 1012 m3 over 1970–2008. Thus, the substantial interannual variability of the Bering Sea ice cover is dominated by changes in the wind-driven ice mass advection and the ocean thermal front at the ice edge. The observed ecological regime shifts in the Bering Sea occurred with significant changes in sea ice, surface air temperature, and SST, which in turn are correlated with the Pacific decadal oscillation over 1970–2008 but not with other climate indices: Arctic Oscillation, North Pacific index, and El Niño–Southern Oscillation. This indicates that the PDO index may most effectively explain the regime shifts in the Bering Sea.
The Bering Sea supports one of the world’s most productive and valuable fisheries, immense populations of marine birds and mammals, and the subsistence activities of native communities (ARCUS 2004). This great biological productivity takes place in a dynamic ocean with substantial seasonal ice cover. Significant changes in the Bering ecosystem have been measured in recent decades. Observations indicate that large-scale ecological “regime shifts” occurred in the Bering Sea during 1976–77, 1988–89, and 1998, affecting the mix and abundance of suites of coexisting species from primary producers to apex predators (e.g., Stockwell et al. 2001; Benson and Trites 2002; Hunt et al. 2002; Hunt and Stabeno 2002). A major ecosystem shift has also been observed in the northern Bering Sea (Grebmeier et al. 2006).
Although our current understanding of the ecological regime shifts in the Bering Sea is not deterministic (Overland et al. 2008), it appears the shifts are closely linked to changes in the Bering climate. Since 1976, surface air temperature (SAT) has generally been increasing, particularly in summer; since 1996, spring consistently arrives earlier. Since 2000, warm SAT anomalies generally extend from February through November (Overland and Stabeno 2004). Long-term moored oceanographic data from the eastern Bering Sea shelf indicate that the depth-averaged spring and summer water temperatures are ∼2°C warmer in the 2001–03 mean than in the 1995–97 mean (Stabeno et al. 2002; Overland and Stabeno 2004). This warming continues until at least 2005 (Stabeno et al. 2007). However, this is not an uninterrupted warming trend; data show that the Bering Sea was very cold in 2008 (see online at http://bsierp.nprb.org/results/headlines.html).
Changes in the Bering climate in the past decades appear to be part of a larger North Pacific shift associated with warmer water temperatures and lower sea level pressures (SLPs) in the winter Aleutian low. Various modes of climate variability have been used to describe changes in Bering climate such as the Pacific decadal oscillation (PDO; Mantua et al. 1997), the North Pacific index (NPI; Trenberth and Hurrell 1994), and the Arctic Oscillation (AO; Thompson and Wallace 1998; Overland et al. 1999). The NPI provides a measure of the intensity of the mean wintertime Aleutian low, whereas the AO is the leading mode of arctic SLP variability that is also linked to the Aleutian low (Stabeno and Overland 2001). The PDO, the leading mode of sea surface temperature (SST) variability in the North Pacific, was in the positive phase from 1977 to the late 1980s, with warmer sea temperatures along the west coast of North America. Recently, the PDO has shifted between negative and positive phases without a persistent pattern. The El Niño–Southern Oscillation (ENSO) events may also influence the eastern Bering Sea through teleconnections (Niebauer and Day 1989; Overland et al. 2001).
A key feature of the Bering marine environment is the sea ice that varies substantially on multiple temporal scales in response to climate change (Niebauer et al. 1999). Winter southwestward ice advection driven by northerly/northeasterly winds and ice melt (IM) at the thermodynamic limit (warm waters in the south) are the principal processes influencing sea ice production/extent in the Bering Sea (Pease 1980). The eastern Bering ecosystem responds strongly to changes in the location of the ice edge and ocean fronts (for an overview, see Macklin et al. 2002). Ice cover affects the availability of light to the water column and the air–sea exchange of biogenic gases. Ice provides both a buoyancy source and sink at the ocean surface, and influences upwelling processes and wind-driven ocean mixing. Sea ice appears also to be important in the formation and maintenance of “cold pools” (Stabeno et al. 2002), regions of cold water in contact with the seafloor that are often associated with high nutrient distributions (Whitledge et al. 1988). The productive “Green Belt” along the Bering Sea slope region, which reflects slope upwelling processes and the shelf–basin exchange of physical and biological properties through currents, eddies, and meanders (Springer et al. 1996; Okkonen et al. 2004), may also be modified by the ice cover. The ice itself is a habitat for a vast range of organisms from ice algae to large marine mammals. Therefore, variability and change in the extent, thickness, and duration of the Bering Sea ice cover will have a major impact on ecosystem functioning and biogeochemical cycling (e.g., Grebmeier and McRoy 1989; Hunt et al. 2002). Thus, it is essential to further our understanding of the behavior of the Bering Sea ice cover in response to climate variability, through field monitoring and numerical model simulations.
A variety of numerical models has been used successfully to study sea ice in the Bering Sea. Some of the models are stand-alone sea ice models (e.g., Pease and Overland 1989). Kantha and Mellor (1989) were the first to use a coupled ice–ocean model to study the Bering Sea marginal ice zone, followed by Pritchard et al. (1990), who aimed to forecast the Bering Sea ice edge. Zhang and Hibler (1991) studied the effect of ocean circulation on seasonal and interannual ice-edge variations in the Bering Sea. Recently, Wang et al. (2009) examined seasonal variations of the Bering Sea ice cover with seasonally varying atmospheric and oceanic conditions. A sea ice model has been coupled to the Regional Ocean Modeling System (P. Budgell 2007, personal communication; available online at http://www.myroms.org/), and the coupled ice–ocean model has been used to simulate sea ice in the Bering Sea (A. Hermann 2008, personal communication; available online at http://www.ecofoci.noaa.gov/efoci_icemodels.shtml). Although these models yield considerable insights about the behavior of sea ice in the Bering Sea, they have not yet been used to quantify the sea ice response to changes in atmospheric and oceanic forcing on interannual and decadal time scales.
We have developed a coupled ice–ocean model, which we refer to as the Bering Ecosystem Study Ice–Ocean Modeling and Assimilation System (BESTMAS). In this paper, we use this model to quantify the interannual and decadal variability of the Bering Sea ice cover over the period 1970–2008. Specifically, we seek to quantify the following: 1) the mechanisms controlling the observed variability of sea ice on interannual and decadal time scales, 2) the effects of the interactions between dynamic and thermodynamic sea ice processes, and 3) the sea ice response to changes in the atmospheric and oceanic forcing. The BESTMAS model is described in section 2. In section 3, we verify the model simulation by comparison with available observations. In section 4, we quantify the various causes of the interannual variability of the Bering Sea ice cover. Concluding remarks are given in section 5.
2. Model description
a. Model components
BESTMAS is based on the coupled parallel ocean and sea ice model (POIM) of Zhang and Rothrock (2003). The sea ice model is the multicategory thickness and enthalpy distribution (TED) sea ice model (Zhang and Rothrock 2001; Hibler 1980). It employs a teardrop viscous-plastic rheology (Zhang and Rothrock 2005), a mechanical redistribution function for ice ridging (Thorndike et al. 1975; Hibler 1980), and a line successive relaxation (LSR) dynamics model to solve the ice momentum equation (Zhang and Hibler 1997). The heat equation is solved over each ice thickness category using Winton’s (2000) three-layer thermodynamic model. The TED ice model also includes a snow thickness distribution model following Flato and Hibler (1995).
The ocean model is based on the Parallel Ocean Program (POP) developed at Los Alamos National Laboratory. The POP model is an advanced version of the Bryan–Cox–Semtner-type ocean model (Bryan 1969; Cox 1984; Semtner 1986). POP includes many improvements such as incorporation of the K-profile parameterization (KPP) scheme for vertical mixing (Large et al. 1994), implementation of an implicit free-surface formulation of the barotropic mode, and adaptation to shared-memory or distributed-memory parallel computers (Smith et al. 1992; Dukowicz and Smith 1994).
Given that tidal energy accounts for 60%–90% of the total horizontal kinetic energy over the southeastern shelf region of the Bering Sea (Kinder and Schumacher 1981), we have incorporated into the POP ocean model the tidal forcing arising from the eight primary constituents (M2, S2, N2, K2, K1, O1, P1, and Q1; Gill 1982). The tidal forcing consists of a tide generating potential with corrections due to both the earth tide and self-attraction and loading following Marchuk and Kagan (1989).
b. Model grid
The model domain of BESTMAS covers the Northern Hemisphere north of 39°N. The BESTMAS finite-difference grid is based on a generalized orthogonal curvilinear coordinate system with a horizontal dimension of 600 × 300 grid points (Fig. 1). The “north pole” of the model grid is placed in Alaska. Thus, BESTMAS has its highest horizontal resolution along the Alaskan coast and in the eastern Bering Sea, with grid spacing ranging from 2 km along the Alaskan coast to 12 km along the Aleutian Chain, with an average of about 7 km for the whole Bering Sea, defined here as the area north of the Aleutian Chain up to Bering Strait (BS). There are 20 grid cells across Bering Strait, which allows a good connection between the Bering Sea and the Arctic Ocean.
The TED sea ice model has eight categories each for ice thickness, ice enthalpy, and snow depth. The centers of the eight ice thickness categories are 0, 0.38, 1.30, 3.07, 5.97, 10.24, 16.02, and 23.41 m. The POP ocean model has 30 vertical levels of varying thicknesses to resolve surface layers and bottom topography. The first 13 levels are in the upper 100 m, and the upper 6 levels are each 5 m thick. The model bathymetry (Fig. 1b) is obtained by merging the International Bathymetric Chart of the Arctic Ocean (IBCAO) and 5-minute gridded elevations/bathymetry for the world (ETOPO5) datasets (see Holland 2000).
c. Forcing and lateral boundary conditions
BESTMAS is forced by daily National Centers for Environmental Prediction–National Center for Atmospheric Research (NCEP–NCAR) reanalysis (Kalnay et al. 1996) surface forcing fields from 1970 to 2008. The reanalysis forcing consists of surface winds, SAT, specific humidity, precipitation, evaporation, downwelling longwave radiation, and cloud fraction. SAT and cloud fraction are used to calculate downwelling shortwave radiation following Parkinson and Washington (1979). Model forcing also includes river runoff of freshwater in the Bering and Arctic Seas. For the Bering Sea, monthly climatological runoffs of the Anadyr, Yukon, and Kuskokwim Rivers are used (see Table 1 for sources). For the Arctic Ocean, monthly climatological runoffs of the Pechora, Ob, Yenisei, Olenek, Yana, Indigirka, Kolyma, Mackenzie, Dvina, Lena, Khatanga, Taimyra, and Piasina Rivers are from the Alfred Wegener Institute (Prange and Lohmann 2004) based on data from the Global River Data Center in Koblenz, Germany (see also online at http://efdl.cims.nyu.edu/project_aomip/forcing_data/rivers/overview_awi.html).
Although BESTMAS has a large model domain that includes the Arctic and the North Pacific, realistic lateral open boundary conditions are still necessary to create the right water masses and transports in the Bering Sea. We have modified the POP ocean model to incorporate open boundary conditions so that BESTMAS is able to be one-way nested to a lower-resolution but global POIM (Zhang 2005). Monthly-mean open boundary conditions of ocean temperature, salinity, and sea surface height from the global POIM are imposed at the southern boundaries along 39°N.
3. Model results and observations
The BESTMAS model is initialized from the global POIM sea ice and ocean conditions of 1 January 1969 (Zhang 2005). BESTMAS is then integrated from 1969 to 2008 using the daily NCEP–NCAR reanalysis forcing. Because we consider the first year as still in spinup mode, we present here results for the Bering Sea over the period 1970–2008. We evaluate model results by comparisons to available observations.
a. Sea ice extent and thickness and model–data comparisons
Figure 2 shows the simulated and observed seasonal and interannual variations of monthly-mean sea ice extent over 1970–2008. The simulated seasonal cycle of ice coverage is generally in phase with the observed cycle, with a few exceptions: model-simulated ice advance in the fall (October–December) and winter (January–March) of 1984 and 1985 is about one month later than observed. The model agrees with the observed winter ice extent maximum, with a 2% bias in March ice extent (Fig. 3a). However, it tends to underestimate the onset of ice in November–January and then overestimate ice extent during April–May (Fig. 3a), mainly in the western Bering Sea (Fig. 4c). Despite this, the interannual variability is reasonably close to observations; the monthly model–data correlation from January to May over 1970–2008 ranges from 0.6 in January to 0.8 in May (Fig. 3a).
The simulated 1970–2008 mean ice thickness averaged over the entire ice extent in the Bering Sea is generally below 1.2 m (Fig. 3b), and the simulated local ice thickness is generally less than 2.5 m (Fig. 4). The simulated sea ice is significantly thinner along the southern coasts of the St. Lawrence (63.42°N, 170.40°W) and St. Matthew (60.42°N, 172.75°W) Islands than in the surrounding areas (Fig. 4), indicating the effects of winter polynya formations that are often observed in those coastal areas (e.g., Stringer and Grove 1991; Grebmeier and Cooper 1995). There are very few ice thickness measurements in the Bering Sea available for model validation. Two moored upward-looking sonars (ULSs) were deployed south of St. Lawrence Island in 1999 as part of a winter polynya field experiment (Drucker et al. 2003), which yielded ∼4-month records of ice thickness. Figure 5 shows a comparison of the model-simulated daily-mean ice thicknesses and the ULS-derived estimates at those two sites (ULS-15 and ULS-42) in the winter of 1999. The model catches some of the ULS-observed ice thickness peaks (e.g., around days 23 and 63) but misses some of the other peaks (e.g., days 29 and 84). The model simulates two peaks between days 42 and 54 that occur 1 or 2 days earlier than the observations. Both model results and ULS measurements show considerable daily variability in ice thickness, reflecting the dynamic nature of the Bering Sea ice cover. The sharp increase in ULS-measured ice thickness on days 44 and 52 is likely a buildup of ridged ice (Drucker et al. 2003). BESTMAS simulates ice ridging and reproduces these two observed ice thickness peaks with some success, suggesting that it is important to incorporate ice ridging processes in models to capture the sometimes large change in ice thickness on daily time scales.
b. Ocean circulation and transports, tidal effects, and model–data comparisons
The general pattern of Bering Sea ocean flows is comparatively well known from observations (Stabeno et al. 1999). The BESTMAS model captures basic features of the observed major currents in the Bering Sea, such as the Alaskan Stream, the Aleutian North Slope Flow, the Bering Slope Current, the Kamchatka Current, and the on-shelf flows (Fig. 6; see also Fig. 2 in Stabeno et al. 1999). The model has inflows through the Aleutian passes and outflow through Bering Strait (described later). The model shows considerable seasonal variability in the strength of the 15-m ocean circulation (Figs. 6a,b), with all the major currents being significantly stronger in winter than in summer. This seasonal change in ocean circulation is generally attributed to a seasonally variable Pacific–Arctic SLP head and seasonally varying wind circulation (Wang et al. 2009).
The incorporation of tidal forcing (section 2a) in the model is found to modify the simulation of ocean flows through tidal rectification. For example, tidal forcing induces a strong clockwise circulation around the Pribilof Islands (Fig. 7a), which is qualitatively in agreement with Kowalik and Stabeno (1999) and Hermann et al. (2002). Without tidal forcing, such a clockwise circulation is not simulated (Fig. 7b). Tidal forcing also influences the simulation of ice thickness. The difference in simulated ice thickness with or without incorporating tidal forcing is often up to 0.1 m or 15% over a large area in the Bering Sea (Fig. 8). The difference is particularly noticeable in the central-eastern Bering Sea, where tides are strong (Kinder and Schumacher 1981). This is because tides affect ice motion and deformation (Pearson et al. 1981), and therefore spatial redistribution of ice mass. Tides also alter the spatial redistribution of ice mass by modifying ocean flows (Fig. 7). For example, by examining the difference in the ocean surface velocity between the simulations with and without tidal forcing, we have found that the velocity difference vectors tend to drive ice into the area north of St. Matthew Island and out of the area southwest of St. Lawrence Island. This leads to thicker ice north of St. Matthew Island and thinner ice southwest of St. Lawrence Island (Fig. 8).
A transect roughly parallel to the shelf break in the central Bering Sea (transect A in Fig. 1) is used to examine the effect of on-shelf oceanic volume and heat transports on changes in sea ice in the Bering Sea. Because river water mass is not added into the model domain but is simulated by changing ocean salinity in the model, the simulated net volume transport across transect A must, by mass conservation, balance the outflow at Bering Strait (Fig. 9a). The simulated 1970–2008 annual-mean outflow at Bering Strait is 0.75 Sv (1 Sv = 106 m3 s−1), in good agreement with the observational estimate of about 0.8 Sv (Roach et al. 1995). Observations of the Bering Strait outflow show significant interannual variability (Woodgate et al. 2005, 2006), which is generally well captured by the model, at least within observational error bars (Fig. 9a).
Like the vertically integrated volume transport, the vertically integrated on-shelf heat transport across transect A (HTA; calculated relative to −1.8°C) also shows significant interannual variability (Fig. 9b). The January–May mean on-shelf heat transport is significantly correlated with the corresponding volume transport (R = 0.64). Not surprisingly, the heat transport is also significantly correlated with the simulated SST over the whole Bering Sea and with the PDO that represents a significant portion of SST variability over the whole North Pacific (Table 2). However, both the simulated heat transport at transect A and SST in the whole Bering Sea are not significantly correlated (R < 0.4) with some other climate indices such as AO, NPI, and ENSO over 1970–2008; therefore, the corresponding correlation values are not listed in Table 2.
c. SST, SAT, and model–data comparisons
Figure 10a compares the simulated May SST in the southeastern Bering Sea with that from NCEP–NCAR reanalysis. The NCEP–NCAR reanalysis SST is derived from the global daily high-resolution Reynolds SST analyses using satellite and in situ observations (Reynolds and Marsico 1993; Reynolds et al. 2007; Kalnay et al. 1996). BESTMAS captures most of the variability in the observation-derived May SST, with a correlation of R = 0.79. The simulated annual or January–May mean SST in the whole Bering Sea is strongly correlated with the corresponding NCEP–NCAR reanalysis SAT (Figs. 10b,c; Table 2), which is not surprising because the latter is a key component of the model forcing. Both SAT and SST averaged over the whole Bering Sea show that winter 1976 is the coldest over the period 1970–2008, whereas the winters of 1979 and 1996 are the warmest (Fig. 10c). Since 2005, the Bering Sea has been cooling significantly and winter 2008 is one of the coldest, whereas winter 2007 SAT is close to the 1970–2008 average.
The different winter conditions of four sample years of 1976 (cold), 1996 (warm), 2007 (average), and 2008 (cold) are illustrated in Fig. 11, which plots fields of winter surface temperature and SAT. Here, surface temperature is the temperature on the sea ice surface or the ocean surface. Thus, the surface temperature south of the ice edge (indicated in Fig. 11) is SST. SST under the ice is close to the freezing point (−1.8°C in the model). The spatial pattern of the simulated surface temperature is generally in agreement with that of the NCEP–NCAR reanalysis surface temperature (note some irregularities in the reanalysis data for winter 1976 near 61°N, 176°E, where the reanalysis surface temperature does not match the observed ice edge; Fig. 11b). The spatial pattern of either simulated or reanalysis surface temperature is in turn close to that of the reanalysis SAT, indicating the effect of air–ice–sea interactions. However, in a large area immediately south of the ice edge, both the simulated and observed SSTs are generally above zero, even though SAT is below zero, particularly in the cold winters of 1976 and 2008. This is because of the significant heat storage in the ocean mixed layer in summer and heat supply in fall and winter to the mixed layer through vertical mixing (Stabeno et al. 2009) and northward heat transport (Clement Kinney et al. 2009; see also Fig. 9b), which is greater than the surface heat loss resulting from winter atmospheric cooling.
d. Interannual variability of sea ice
Figures 12a,b illustrate the interannual variability of the Bering Sea ice cover by showing time series of ice extent and volume averaged over January–May, a period when a significant portion of the Bering Sea is covered by ice (Fig. 3). In general, the model performs well; it overestimates the January–May mean sea ice extent by only 3% on average over the period 1970–2008 (Fig. 12a). It also captures well the variability of observed ice extent (OIE) with a model–data correlation of R = 0.78 and a root-mean-square (RMS) error of 13%. The simulated total ice volume in the Bering Sea (Fig. 12b) is similarly correlated with the observed ice extent (R = 0.76; Table 2); as expected, it is even more strongly correlated with the simulated ice extent (R = 0.96). Both ice extent and ice volume reflect the substantial interannual differences of the Bering Sea ice cover (Figs. 12a,b). Being the coldest year over 1970–2008, 1976 has the highest total ice volume and its ice cover is generally thicker over a larger area than other years such as 1996 (warm), 2007 (average), and 2008 (cold; Fig. 13). Conversely, 1996, a warm year, has the second lowest ice volume, and St. Matthew Island is almost ice free in winter (Fig. 13b). The simulated ice volume (SIV) in the Bering Sea increases gradually from 1979 to 1995 and then drops steeply in 1996. It doubles from 1996 to 2000 and then decreases significantly from 2000 to 2005. From 2005 to 2008, the ice volume and extent recover, and 2008 is one of the heaviest ice years (Figs. 12a,b, 13d).
4. Quantifying the causes of sea ice interannual variability in the Bering Sea
a. Changes in sea ice with varying SAT and SST
Bering Sea sea ice variability is due to the interplay among the climate components of the atmosphere, ocean, and sea ice itself. For example, the 2000–05 warming in the southeastern Bering Sea shelf occurred in conjunction with a mild air mass during the winter and a shorter ice season (Stabeno et al. 2007). Over the period 1970–2008, the January–May mean simulated ice volume and observed ice extent are highly negatively correlated with the corresponding reanalysis SAT (Table 2); the two time series of ice volume and SAT (also plotted in Fig. 10c) are almost symmetric horizontally (Fig. 12b). Lower SAT, often in association with lower downward longwave radiative flux (not shown), causes stronger surface cooling, leading to greater ice growth (IG). The opposite is true with higher SAT. For example, the 1976 maximum ice volume/extent occurs when both the January–May mean SAT drops to the lowest point in the record (Fig. 12b) and the winter SAT is below 0°C over almost the entire Bering Sea (Fig. 11c). Conversely, winter 1996 has a lower than usual ice volume and a higher than usual SAT (Figs. 11f, 12b). The increase (decrease) in ice volume during 2000–05 (2005–08) is associated with increasing (decreasing) SAT.
The simulated ice volume and observed ice extent are also correlated with the simulated SST in the Bering Sea and PDO, which represents a significant portion of the observed SST variability in the North Pacific (Table 2). This suggests that ocean heating may have an important role in defining ice extent and affecting ice thickness. On the other hand, the ice cover has an equally important role in modifying SST such that an ocean thermal front often forms along the ice edge, as is demonstrated by the close match between the simulated SST front and the location of the observed ice edge (Fig. 11). The simulated ice volume and observed ice extent, like the simulated on-shelf heat transport at transect A and SST averaged in the whole Bering Sea, are found to correlate poorly with other climate indices such as AO, NPI, and ENSO over 1970–2008, with correlation values generally below 0.3. This suggests that these climate indices are not particularly skillful at determining changes in the Bering Sea.
b. Changes in sea ice with varying atmospheric circulation
Wind circulation affects Bering Sea ice motion and ice mass advection. Ice motion is described by ice velocity, whereas ice mass advection is described here by ice mass convergence [−∇ · (uh)], where u is ice velocity and h is ice thickness. Thus, changes (loss or gain) in ice thickness due to ice mass advection (or ice mass convergence) quantitatively describe the effects of wind-driven ice motion and deformation on the spatial redistribution of ice mass. In winter, considerable ice loss due to ice mass advection (ILDA) generally occurs in the north and east of the Bering Sea, whereas ice gain occurs in the south and west (Fig. 14), indicating a large-scale ice movement from north and east to south and west, as described by Pease (1980). Local changes (loss or gain) in ice thickness due to ice mass advection can be up to ±0.5 m month−1. This general pattern of ice mass advection tends to expand ice extent southward significantly (Fig. 14).
Such an ice mass advection pattern is attributed to strong southwestward ice motion (Fig. 14) driven primarily by the strong northeasterly winds prevailing in winter (Pease 1980). Surface ocean circulation has a secondary role in ice mass advection because it is often in the opposite direction of ice motion (Figs. 6a, 14). The winter atmospheric circulation in the Bering Sea is often characterized by relatively high SLP in the west and north and low in the east and south because of the formation of a high pressure cell over a large area in Russia and a low pressure cell over the Aleutian Islands, leading to generally strong northeasterly winds in winter as these cells intensify (Figs. 15a–d; Pease 1980; Trenberth and Hurrell 1994; Niebauer et al. 1999; Overland et al. 1999). The strong winds, in conjunction with generally thinner ice of less strength, cause the simulated speed of winter ice motion in the Bering Sea (Fig. 14) to be greater than that in most of the Arctic Ocean (Zhang and Rothrock 2003).
One effect of the wind-driven ice mass advection is that ice is moved away from the areas downwind of the St. Lawrence and St. Matthew Islands and piled up in the areas upwind of these islands (Fig. 14; see also Pease 1987). This is illustrated by ice loss (blue color) to the south of these islands and ice gain (red color) to the north (Fig. 14). Also, ice mass advection as well as ice ridging are likely to cause the sometimes substantial daily variability in ice thickness simulated by the model and measured by the ULSs deployed in the polynya area south of St. Lawrence Island in 1999 (Fig. 5; Drucker et al. 2003).
On average over 1970–2008, the total ice loss (gain) due to ice mass advection during January–May in mainly the north and east (south and west) of the Bering Sea is about 1.4 × 1012 m3 over the 5-month period (Fig. 12c). This amount is almost twice that of the January–May mean total ice volume (0.76 × 1012 m3; Fig. 12b). In other words, on average, almost twice as much ice as the total ice volume moves from north and east to south and west of the Bering Sea. Note that the simulated 1948–2000 annual-mean sea ice export from the Arctic Ocean to the subarctic seas (mainly through Fram Strait) is about 2.7 × 1012 m3 yr−1 (Rothrock and Zhang 2005), and BESTMAS estimates that the January–May mean ice export at Fram Strait over 1970–2008 is 1.3 × 1012 m3 over the 5-month period. This means that the north/east to south/west ice mass advection during January–May in the Bering Sea is comparable in magnitude to the arctic ice export at Fram Strait.
The amount of ice moving southwestward fluctuates considerably from year to year because of the substantial interannual variability of the winter northeasterly winds, which are linked to the location and intensity of the Russian high pressure and Aleutian low pressure centers (Fig. 15; see also Overland et al. 1999). The extent and thickness of the ice cover in the southern Bering Sea are controlled by the magnitude and pattern of ice mass advection, which contributes to either an increase or a decrease of more than half of the long-term January–May mean ice volume (0.76 × 1012 m3). During the heavy ice years of 1976 and 2008 (Figs. 13a,d), ice mass advection is stronger and more expansive than usual and a large area south of 60°N gains ice due to ice mass advection (Figs. 14a,d), with a total ice gain up to 1.8 × 1012 m3 in 1976 (Fig. 12c). This is because the northeasterly winds in winter 1976 and 2008 are stronger than usual such that the wind anomaly vectors have a significant southward component over a large area, particularly south of 60°N (Figs. 15e,h). In 1996, one of the lightest ice years (Fig. 13b), the amount of ice being advected (0.98 × 1012 m3; Fig. 12c) is among the lowest and there is little ice gain in the area south of 62°N (Fig. 14b). This is because the northerly winds are so weak that the wind anomaly vectors are strongly northward (Fig. 15f). There is more ice in 2007 than in 1996, and ice mass advection in 2007 is somewhat stronger than in 1996 because of relatively stronger northerly winds or a weaker northward wind anomaly (Figs. 13c, 14c, 15g).
The close link between the wind-driven ice mass advection and ice extent/thickness is further shown by the significant correlation between the simulated ice volume and observed ice extent and the total ice loss due to ice mass advection (Fig. 12c; Table 2). The total ice loss due to ice mass advection is also correlated with the northerly wind velocities (NWV) averaged over the Bering Sea (R = 0.48; Table 2). All this suggests that atmospheric circulation, through ice mass advection processes, has a dominant role in shaping the Bering Sea ice cover. However, the correlation between the northerly wind velocities and the simulated ice volume or observed ice extent is not significant (Table 2). This suggests that the total ice loss or gain due to ice mass advection is a better proxy to describe winter sea ice response to wind forcing than wind velocities themselves.
c. Effects of the interactions among dynamic and thermodynamic sea ice processes
Ice production is a useful parameter to quantify the effects of the interactions among dynamic and thermodynamic sea ice processes. Here, ice production (Fig. 16) represents the net effects of all the air–ice–ocean thermodynamic processes modified by dynamic processes such as wind-driven ice mass advection (Zhang et al. 2008). Generally, winter ice production is strongly positive in the northern Bering Sea, indicating substantial thermodynamic ice growth that can be up to 0.5 m month−1 locally. On average over 1970–2008, the total ice growth during January–May is 1.4 × 1012 m3, close to the total ice loss or gain due to ice mass advection. The strong growth is attributed to surface atmospheric cooling with SAT much lower than 0°C (Fig. 11). The northern Bering Sea is also subject to significant ice loss due to wind-driven southward ice mass advection (Fig. 14). As ice moves southward, a greater area of open water/thin ice is created in the north, which enhances ice growth because growth rates over open water/thin ice are higher than over thick ice (e.g., Maykut 1982). Thus, the strong thermodynamic growth in the north is attributed to the combined effects of atmospheric cooling and ice opening up because of ice mass advection. This is why the January–May mean simulated total ice growth (Fig. 12d) is strongly correlated with both the January–May mean SAT (Fig. 10b; Table 2) and the total ice loss (gain) due to ice mass advection January–May (Fig. 12c; Table 2).
Southward ice mass advection also induces thermodynamic ice melt. Although winter ice growth is high in the north, significant ice melt occurs in the south, mainly near the ice edge where ice melt can be as high as −0.5 m month−1 with substantial interannual variability (Fig. 16). Given that SAT is generally below 0°C in winter even in a large area south of the ice edge (Fig. 11), it is not atmospheric heating (reflected in SAT) that causes the melting near the ice edge. Rather, it is the oceanic heat that melts the ice as winds drive ice southward into relatively warm surface waters (see also Pease 1980). Note that either the simulated or the reanalysis winter SST near the ice edge is generally above 0°C, even though SAT is below 0°C (Fig. 11). This is because of the significant heat storage in the ocean mixed layer in summer and heat supply in fall and winter to the mixed layer through vertical mixing and northward heat transport. The high (negative) correlation (Table 2) between the on-shelf heat transport across transect A and the simulated ice volume or observed ice extent indicates the importance of northward heat transport, which tends to suppress ice growth in the shelf region. The mixed layer heat contributes to strong melting in the ice-edge areas where there is also a large ice gain due to ice mass advection (Figs. 14, 16). In other words, the combination of ice mass advection and the ocean thermal front at the ice edge largely defines the location of the ice edge or the shape and size of ice extent in winter (see also Pease 1980).
In April and May, SAT increases; as a result, ice melting is more widespread and not mainly confined near the ice edge (not shown). Thus, in spring, atmospheric heating has a more prominent role in ice melting than oceanic heating. This is why the total ice melt January–May in the Bering Sea (Fig. 12d) is closely correlated with the simulated SST and reanalysis SAT (Table 2). It is even more highly correlated with the total ice loss due to ice mass advection (Table 2), indicating again the prominent role of ice mass advection in ice melting in the Bering Sea. On average over 1970–2008, the amount of total ice melt January–May is substantial at 1.5 × 1012 m3, with significant interannual fluctuations (Fig. 12d).
5. Concluding remarks
We have developed a coupled sea ice–ocean model (BESTMAS) to quantify the changes in sea ice processes in the Bering Sea in response to atmospheric and oceanic forcing on interannual and decadal time scales. Although model deficiencies exist at least in part because of uncertainties in model parameterization, forcing, and initialization, the model captures much of the observed seasonal and interannual variations of the Bering Sea ice cover. It also captures the basic features of the upper-ocean circulation and the large-scale spatiotemporal variability of SST in the Bering Sea. Model results suggest the necessity of incorporating ice ridging processes to capture the occasionally large daily change in ice thickness due to ice mass advection and deformation in the polynya area south of St. Lawrence Island. Model results also indicate that tidal forcing affects the spatial redistribution of ice mass by up to 0.1 m or 15% over a large area in the central-eastern Bering Sea by modifying ice motion and deformation and ocean flows.
The strong correlations among the simulated ice volume, observed ice extent, SAT, and SST over 1970–2008 indicate the sensitivity of sea ice to changes in atmospheric and oceanic forcing and the effect of air–ice–sea interactions. Interannual variability is considerable for the Bering Sea ice cover over 1970–2008, during which the region underwent periods of significant cooling and warming according to the reanalysis SAT and the simulated SST. The ice cover responds to the cooling and warming such that the January–May mean simulated ice volume (observed ice extent) can be as high as 1.3 × 1012 m3 (1.1 × 1012 m2) in 1976 or as low as 0.46 × 1012 m3 (0.54 × 1012 m2) in 1996. More recently, SAT–SST decreases during 1996–2000, increases during 2000–05, and decreases again during 2005–08; the ice cover changes accordingly, with a January–May mean simulated ice volume (observed ice extent) of 0.94 × 1012 m3 (0.72 × 1012 m2) in 2000, 0.52 × 1012 m3 (0.55 × 1012 m2) in 2005, and 0.97 × 1012 m3 (0.84 × 1012 m2) in 2008 (one of the heaviest ice years in the record).
As suggested by Pease (1980), changes in ice extent and thickness in the Bering Sea are most profoundly affected by wind-driven ice mass advection processes. The model allows us to quantify these processes. The Bering Sea winter features strong northeasterly winds that drive ice faster than usually observed in the Arctic Ocean, causing ice mass advection comparable in magnitude to the arctic ice export via Fram Strait. On average in the model, about 1.4 × 1012 m3 of ice, almost twice as much as the mean total ice volume in the Bering Sea (0.76 × 1012 m3), moves from the northeast to the southwest of the Bering Sea during January–May, causing significant southward expansion of ice extent. Because the atmospheric circulation varies substantially from year to year, the amount of ice moved fluctuates, from as much as 1.8 × 1012 m3 in the heavy ice year of 1976 to about half of that amount in the light ice year of 1996.
Ice mass advection also interacts with thermodynamic sea ice processes. It enhances thermodynamic ice growth in the north by increasing the areas of open water or thin ice. The average ice growth during January–May is 1.3 × 1012 m3, ranging from 0.90 × 1012 m3 in 1996 to 2.1 × 1012 m3 in 1976. Ice mass advection also enhances thermodynamic ice melting in the south by bringing ice into warm waters, causing considerable ice melting in the ice-edge areas. The average ice melt during January–May is 1.4 × 1012 m3, ranging from 0.94 × 1012 m3 in 1996 to 2.0 × 1012 m3 in 1976. In other words, ice mass advection modifies SST by cooling surface waters and forming a temperature front at the ice edge, whereas oceanic heat constrains the advection-induced southward ice expansion by melting ice near the ice edge. Thus, the interplay between ice mass advection and the ocean thermal front across the ice edge largely defines the shape and size of Bering ice extent (Pease 1980). The substantial amount of ice melting and interannual fluctuations are likely to significantly affect the meltwater distribution and ocean stratification in a large area in the southern Bering Sea, including the slope region (Green Belt) of great biological productivity.
The observed ecological regime shifts during 1976–77 and 1998 are reflected in significant changes in sea ice. The 1976–77 regime shift is associated with the heaviest ice year (1976), and the 1998 regime shift occurred with a significant increase in ice volume after two consecutive light ice years (1996–97). The correspondence between changes in sea ice and the 1988–89 regime shift is less obvious. However, the periods of 1976–77, 1998, and 1988–89, during which ecological regime shifts were observed (e.g., Stockwell et al. 2001; Benson and Trites 2002; Hunt et al. 2002; Hunt and Stabeno 2002), are all marked by significant changes in SAT, SST, and thus the PDO index (Figs. 9b, 10). Changes in sea ice, SAT, and SST all correlate significantly to the PDO but not to the AO, NPI, and ENSO over 1970–2008, indicating that the PDO may explain the regime shifts in the Bering Sea most effectively.
The results provoke speculation on a scenario of Bering Sea air–ice–ocean interactions in winter of a heavy ice year. Generally, a heavy ice year occurs with a relatively greater SLP difference between the western and eastern Bering Sea and stronger northeasterly winds, which drive more ice into the south and west of the Bering Sea, cooling the surface air and the upper ocean and melting ice there. Stronger northeasterly winds also bring more cold air into the Bering Sea from the north, thus further cooling the surface air and the upper ocean. The decreased SAT and the increased creation of open water/thin ice area due to ice mass advection enhance thermodynamic ice growth in a large area in the northern Bering Sea. In addition, because the increased presence of sea ice in the west tends to cool SAT and SST there, the relatively high SLP in the western Bering Sea and on the nearby land (Figs. 15a,d,e,h) may tend to increase further, thus likely strengthening the northerly winds. In a light ice year, a similar but reversed mechanism in the air–ice–ocean interactions in the Bering Sea would occur (Figs. 15b,f). Here, longwave radiation is not mentioned, but its effect is likely similar to that of SAT related to surface turbulent heat flux. Note that such air–ice–ocean interactions are not fully captured by BESTMAS because it is not coupled to an atmospheric model. However, some of the effects of the air–ice–ocean interactions are likely present in the NCEP–NCAR reanalysis atmospheric forcing used to drive BESTMAS.
This work is supported by NSF Grant ARC0611967. We thank R. Drucker for assistance with the ULS ice thickness data, R. Lindsay for constructive comments, and Dr. S. Okkonen for helpful suggestions.
Corresponding author address: Jinlun Zhang, Polar Science Center, Applied Physics Laboratory, College of Ocean and Fishery Sciences, University of Washington, 1013 NE 40th St., Seattle, WA 98105. Email: firstname.lastname@example.org

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Bacon and black coffee for breakfast, or oatmeal and bananas?
If you decided to make a new year’s resolution and try to lose weight in 2019 you are sure to have found a fierce debate online – and among your friends and family – about how best to do it.
It seems as if everyone has an opinion and new fads emerge every year.
Two major studies published in the past year provided more fuel for a particularly polarising topic – the role carbohydrates play in making us fat.
The studies gave scientists some clues, but, like other nutrition studies, they cannot say which diet, if any, is best for everyone.
That is not going to satisfy people who want black-and-white answers, but nutrition research is extremely difficult and even the most respected studies come with big caveats.
People are so different that it is all but impossible to conduct studies that show what really works over long periods.
Before embarking on a weight loss plan for the new year, here is a closer look at some of what was learned last year.
Fewer carbs means less weight?
It is no longer called the Atkins Diet, but the low-carb school of dieting has been enjoying a comeback.
The idea is that the refined carbohydrates in foods such as white bread are quickly converted into sugar in our bodies, leading to energy swings and hunger.
By cutting carbs, the claim is that weight loss will be easier because your body will instead burn fat for fuel while feeling less hungry.
One recent study seems to offer more support for low-carb proponents. But, like many studies, it tried to understand only one sliver of how the body works.
The study, co-led by an author of books promoting low-carb diets, looked at whether varying carb levels might affect how the body uses energy.
Among 164 participants, it found that those people on low-carb diets burned more total calories than those on high-carb diets.
The study did not say if people lost more weight on a low-carb diet – and did not try to measure that. Meals and snacks were tightly controlled and continually adjusted so everyone’s weight stayed stable.
David Ludwig, a lead author of the paper and researcher at Boston Children’s Hospital, said the study suggests limiting carbs could make it easier for people to keep weight off once they have lost it. He said the approach might work best for those with diabetes or pre-diabetes.
Ludwig said the study was not intended to test long-term health effects or real-world scenarios where people make their own food. The findings also needed to be replicated to be validated, he said.
Caroline Apovian of Boston University’s School of Medicine said the findings were interesting fodder for the scientific community, but that they should not be taken as advice for the average person looking to lose weight.
Do I avoid eating fat to be skinny?
For years people were advised to curb fats, which are found in foods including meat, nuts, eggs, butter and oil. Cutting down on fat was seen as a way to control weight, since a gram of fat has twice as many calories than the same amount of carbs or protein.
Many people say the advice had the opposite effect by inadvertently giving us a licence to gobble up fat-free biscuits, cakes and other foods that were full of the refined carbs and sugars now blamed for our wider waistlines.
Nutrition experts gradually moved away from blanket recommendations to limit fats for weight loss.
Fats are necessary for absorbing important nutrients and can help us feel full. But that does not mean you have to live on eating steak drizzled in butter to be healthy.
Bruce Y. Lee, a professor of international health at Johns Hopkins University in the US, said the lessons learned from the anti-fat fad should be applied to the anti-carb fad: don’t oversimplify advice.
“There’s a constant look for an easy way out,” Lee said.
So which is better?
Another big study over the past year found low-carb diets and low-fat diets were about equally effective for weight loss. Results varied by individual, but after a year people in both groups shed an average of 12 to 13 pounds (5.4 to 5.9 grams).
The author said the findings do not contradict Ludwig’s low-carb study. Instead, they suggest there may be some flexibility in the ways we can lose weight.
Participants in both groups were encouraged to focus on minimally processed foods such as produce and meat prepared at home. Everyone was advised to limit added sugar and refined flour.
“If you got that foundation right, for many, that would be an enormous change,” Christopher Gardner, of Stanford University, who was one of the study’s authors, said.
Limiting processed foods could improve most diets by cutting down overall calories, while still leaving room for people’s preferences.
That is important because for a diet to be effective, a person has to be able to stick to it. A breakfast of fruit and oatmeal may be filling for one person, but leave another person hungry soon after.
Gardner said the study had its limitations, too.
Participants’ diets were not controlled. Instead, people were told how to achieve eating a low-carb or low-fat in regular meetings with dietitians, which may have provided a support network most dieters do not have.
So, what works?
In the short term you can probably lose weight by eating only raw foods, or going vegan, or cutting out gluten, or following another diet plan that catches your eye.
However, what will work for you over the long term is a different question.
Zhaoping Li, director of the clinical nutrition division at the University of California, Los Angeles, said there was no single set of guidelines that helped everyone lose weight – and to keep it off. It’s one reason diets often fail – they do not consider the many factors that drive us to eat what we do.
To help people lose weight, Li looks at their eating and physical activity routines to identify improvements they will be able to live with.
“What sticks is what matters,” Li said.

domain: medical


By Angelo M. Codevilla
Posted May 5, 2001
This article appeared in the Wednesday, May 9th, 2001 edition of the Wall Street Journal.
President Bush's decision to walk away from the 1972 U.S.-Soviet Anti-Ballistic Missile Treaty, while reducing U.S. nuclear forces as he thinks best, removes a major obstacle to missile defense and augurs the end of arms control as a plank of U.S. policy. Yet before America can have a missile defense the Bush administration must fix the mess of missile-defense programs run for years by managers who sought arms control more than defense.
The administration must also make room within a Pentagon that is ignorant of, and opposed to, missile defense, for some entity with the incentive to create and operate the needed devices. Defense Secretary Donald Rumsfeld's proposal yesterday for an overhaul of the Pentagon's space programs, including a new post for an Air Force general to oversee them, may be a good start.
But opposition will come from a politically liberal subculture in American universities, think tanks, and the U.S. government that now risks irrelevance. It is significant that in the broadcast commentaries that followed the president's recent speech, people like MIT's Theodore Postol, who have made careers of opposing missile defense, denied being opposed to missile defense or even being arms controllers. Rather, they stressed their official relationships with U.S. programs and argued that missile defense is just not feasible.
In a sense, they are correct. If the administration bases its plans on existing missile-defense programs (as shaped by eight years of malevolent mismanagement), if it does not understand the many ways in which the assumptions of arms controllers have made these programs the weak things they are today, and if it simply entrusts them, and more money, to the same people and organizations, the legacy of arms control will continue to deprive America of missile defense.
The ABM legacy that weighs heaviest on the effectiveness of interceptors based on the ground or at sea is that, as of now, the interceptors must receive target maps and battle-
management directions from surface-based radars and computers. Our low-orbit network of heat-sensing satellites is now planned merely to augment such arrangements. This makes for gross inefficiency. All surface-based information and battle-management systems can begin to work only when they first see warheads coming over the horizon. But by the time this happens, there is too little time to intercept fast warheads as far enough away as we would like.
Moreover, such arrangements require that the homing mechanism that guides the interceptors also be able to discriminate between warheads and decoys. Homing devices are inherently unsuited for this. As long as we stick with this way of doing things, we will be trying to make homing devices smarter than they can be, and we will be making certain satellites dumber than they could and should be.
The efficient way to use interceptors based on land or at sea is to feed them target maps and battle management directly from our planned network of low-orbit, heat-sensing satellites. But to do that, they must be equipped with software and communication packages different from the ones now planned.
The legacy of arms control has also deformed our programs for using lasers to intercept missiles during boost phase, as they rise from their launchers. The Clinton administration's favorite program involves putting a laser gun on Boeing 747 aircraft and flying them near suspected missile-launch sites, waiting for the missiles to go up. The technical difficulties of creating vacuums for each shot, stabilizing the device, and trying to push the beam through unpredictable atmospheric conditions are horrid. The thought of perpetual air patrol stations over or near hostile countries is silly. But the arms controllers love the airborne laser not because of what it can do badly, but because of what it cannot do at all, namely reach into Russia or China. Will the Bush administration know better?
The only other U.S. program for boost-phase defense, the Space Based Laser (SBL), has been the arms controllers' No. 1 bete noire precisely because it would effectively strike missiles originating anywhere. President Clinton included a specific ban on this weapon in his 1997 attempt to expand the ABM Treaty. Because the SBL had long since met all technical requirements and was ready for flight demonstration, the Clinton administration recycled it into research, where it has been loaded with new requirements and delayed until 2013. Any effort to rescue the SBL would have to proceed from knowledge of technical booby traps laid, and of technical opportunities forgone.
Not least of the legacies of the ABM Treaty is the Pentagon bureaucracy's lack of seriousness about missile defense. The services cannot accommodate missile defense within themselves. For almost half a century, all have sought pieces of the mission primarily to keep money from going to other services.
With the partial exception of the Army in the late 1960s, the services have seen missile defense as an alien, money-sucking body threatening to grow within themselves, and missile-defense money as a pot from which to draw for other purposes.
The Reagan administration established a unit within the Pentagon, since renamed the Ballistic Missile Defense Organization (BMDO), to do research on missile defense. But the BMDO cannot turn itself into the builder of U.S. missile defense because its personnel are assigned by, and loyal to, the services rather than to the mission. Building a missile defense is going to take something like Adm. Hyman Rickover's nuclear navy program — still resented by the Navy a half century afterward — or some unit that begins within one of the services and evolves into a separate service, or a brand new unit directly under the secretary of defense.
Mr. Rumsfeld's announcement of a revitalized Air Force Space Command opens the possibility of such a unit. From its inception in 1984, Space Command's mission has included controlling space — meaning defending U.S. satellites, attacking enemy satellites, and preventing enemy weapons from transiting space. Logically that includes stopping ballistic missiles, which must fly through space.
But Space Command has never had any weapon for doing such things. Both national policy and its status as the junior command in its service prevented it from even asking for such weapons. It so happens that some of the weapons necessary for space control, notably the SBL, would also be excellent for missile defense. If Mr. Rumsfeld were to order this command to develop the weapons it needs for its mission, give it direct access to top civilian officials, as well as a future beyond the Air Force, missile defense might just happen.
So President Bush has effectively renounced the ABM Treaty. Now let's see if his administration can deliver America from its legacy.
Note: The Bush Administration gave its six month notice of withdraw from the ABM Treaty in December of 2001.


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It’s All a Little Poopy: Toxoplasmosis in Cats
Scoop cat poop early and often — and keep their poop away from your garden.
Your pet wants you to read our newsletter. (Then give them a treat.)
If you’re the kind of person who Googles, “My cat is sick; can I catch it?” every single time your cat looks even a little puke-y, you’re going to want to read ahead. There are a handful of diseases that you can catch from a cat, usually from infected feces, infected skin, or bites and scratches. One of the most commonly discussed is toxoplasmosis, one of the poop-related diseases.
This disease was once considered so worrisome that physicians would recommend that pregnant people rehomeopens in a new tab their cats. The Centers for Disease Control (CDC) now statesopens in a new tab that you can keep your cat and just take general precautions instead. Let’s review what toxoplasmosis is, how cats get it, how people get it, and how to avoid getting it without getting rid of your cat.
What is toxoplasmosis and how do cats get it?
Toxoplasmosis is an infection caused by microscopic protozoa — single-celled organisms — called Toxoplasma gondii. Toxoplasmosis can affect mammals, including humans, and is of particular concern in households with cats.
Cats are the definitive hosts for Toxoplasma gondii, meaning they are the only species in which the parasite can sexually reproduce. Cats become infected by ingesting birds, small mammals, or raw/undercooked meat infected with tissue cysts. The parasite completes part of the reproductive process within the cat, then the cat sheds oocysts (thick-walled cells that contain fertilized eggs) in their feces. These oocysts contaminate the environment where the cat poops — soil, water, or litter box — and become infective after one to five days.
Animals in the environment, often birds, small mammals, or livestock, become infected by ingesting the oocysts from contaminated soil or water. The oocysts will burst open within these animals and form cysts in their muscle tissue, restarting the cycle.
What are the symptoms of toxoplasmosis in cats?
Healthy adult cats may have a short bout of diarrhea at worst, but most cats infected with Toxoplasma gondii don’t show any symptoms. Young kittens and cats with compromised immune systems have a greater risk of developing clinical signs associated with the parasite dividing and migrating through the body.
Young kittens with toxoplasmosis will display a general failure to thrive known as “fading kitten syndrome.” These kittens are often born underweight and have difficulty feeding and maintaining normal body temperatures. Without (and sometimes despite) significant nursing care, they often don’t survive. Toxoplasmosis symptoms seen in cats of all ages can include:
Vomiting and Diarrhea
Jaundice (yellowing of the skin or eyes)
Uveitis (inflammation within the eye)
Neurological signs (including seizures, trouble walking, behavior changes, paralysis)
Miscarriage or stillbirth in pregnant cats
How do you diagnose toxoplasmosis in cats?
Because most cats do not show any symptoms of infection, many Toxoplasma infections go undetected. Even when infection is suspected, confirmation can be difficult. Usually, a combination of medical history, clinical signs, blood work, and response to treatment are used to make a diagnosis. Antibody levels may be measured to determine likelihood of current disease, previous exposure, or risk of future exposure.
How do you treat toxoplasmosis in cats?
Antibiotics are the primary treatment for toxoplasmosis in cats. In addition to antibiotics, your vet may recommend secondary treatments to address inflammation in the eyes or central nervous system. Depending on the severity of disease, supportive care may be required to address dehydration, anorexia, nausea, or discomfort.
With appropriate treatment, most cats show noticeable improvement within 72 hours. Prognosis is worse in young kittens, immunocompromised cats, and cats that develop neurologic symptoms. Even if a cat’s symptoms resolve, medication cannot fully eliminate the organism from the tissues. This means that recurrence is possible, though rare.
The solution: Scoop the poop early and often.
All humans are at risk for being infected by Toxoplasma gondii. Similar to cats, people with healthy immune systems typically don’t have any symptoms. Humans can get infected through contact with infected cat feces, by ingesting undercooked and infected meat, by drinking infected water, in utero, and (very rarely) through transfusions and transplants.
Let’s focus on the cat crap for a minute. Because cats infected with Toxoplasma gondii will shed oocytes in their feces, anyone who handles cat feces is at risk for exposure. The most obvious point of contact is the litter box. A less commonly considered exposure is gardening or consuming home-grown produce if neighborhood cats use the garden as a litter box. Outdoor cats may also use playground sandboxes as giant litter boxes, creating a point of exposure for children.
Becoming infected with Toxoplasma gondii during pregnancy carries the risk of passing the parasite on to the fetus, which can result in a condition called congenital toxoplasmosis. Congenital toxoplasmosis can result in blindness, neurological disease, mental disorders, or stillbirth. People infected with Toxoplasma while pregnant may experience flu-like symptoms or no symptoms at all.
People can also take multiple precautions to avoid getting Toxoplasma from cats, especially those who are pregnant or immune-compromised. People who enjoy gardening and garden-fresh produce should wear gloves while gardening and wash their hands afterward. The produce should also be carefully washed. Because it takes at least 24 hours for the oocysts in cat feces to become infective, litter boxes should be cleaned daily to minimize risk. If possible, those who are pregnant or immune-compromised should avoid litter box duties completely.
You can protect your cat from Toxoplasma by feeding a cooked, commercial diet. Keeping your cat indoors prevents them from hunting small prey animals like birds and rodents that may have infected tissue cysts.
Dr. Alycia Washington, DVM, MS
Alycia Washington, DVM, is a small animal emergency veterinarian based in North Carolina. She works as a relief veterinarianopens in a new tab and provides services to numerous emergency and specialty hospitals. Dr. Washington is also a children’s book author and freelance writer with a focus on veterinary medicine. She has a special fondness for turtles, honey bees, and penguins — none of which she treats. In her free time, Dr. Washington enjoys travel, good food, and good enough coffee.
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9 Diseases You Can (and Definitely Can’t) Catch From Your Dog
Here’s what you can scratch off your “Worry About This” list.
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Finally, a Litter Box That’s Thought of Everything
An electric litter box for techy cat parents and their tactful felines.
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Litter Robot: Will My Cat Use an Automatic Litter Box?
I introduced my cat to an automatic litter box, and let’s just say it went off with multiple hitches.
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How to Deal with Cat Diarrhea
Dr. Audrey K. Cook’s tips to getting to the bottom of a sh*tty situation.

domain: health


Hundreds of axed post offices may be reopened after a council's pioneering £1.5million rescue plan.
Town Hall chiefs are using the cash from council tax to run 15 of Essex's 31 closed branches.
The axed Station Way branch in Epping Forest opened its doors again last week and will be used as a model for other rescues.
Around 100 other councils have now approached Post Office Ltd to discuss following the Essex example. Half have signed "nondisclosure" agreements, allowing them to look at the books of threatened or closed branches. A dozen are in advanced talks about saving them.
They include branches in Lewisham and Haringey in London, Darlington and Leicester.
Elaborate measures have been taken to ensure that the deal does not break EU rules on Government subsidies. Under the agreement, the traditional Post Office logo is blacked out and official signs are banned in the branch.
The idea came about after Local Government Minister John Healey wrote to council chiefs suggesting they offer a lifeline.
An industry insider said yesterday: "This could mean Post Office services are kept in hundreds of communities."
A Post Office spokesman said: "We will consider any viable proposal put to us by a local authority."
Around 2,500 post offices are being axed to cut the 14,300- branch network to stem losses.


Our extensive range of testing equipment is always the very latest available, ensuring we stay in touch with technological advancements and provide results with maximum benefits to the athlete. Below are some examples of the technology you might experience during a testing day:
World Leading Wireless Timing Gate System
Sports performance is a lot more complicated than how fast an athlete can run and our timing gates allow athletes to truly understand sport specific speed, agility, power and endurance. Hundreds of the world’s most famous professional teams are turning to similar timing gates on a daily basis for training, testing, research and teaching.
Light Training/Testing System
Flexible, wireless light training/testing system that can be adapted to work and test a wide range of attributes, the main one being hand/eye coordination. Others include speed, strength and the ability to concentrate.
Plyometric Jumping System
Jump force mat with hand held computer displays height and hang time for one jump, ground contact time for one jump and average height and flight time for several jumps. Plyometric mode allows us to compute foot quickness, explosive leg power and a fatigue factor rating.
Hydraulic & Digital Dynamometers
Accurate and safe method of measuring strength in all athletes. Covering the legs, back and arms we can gage average strength along with individual area results.
Concept2 Rowing Machine
Using a short and intense test with our rowing machine we measure full body power.
KMS Foot Speed System
Measuring foot speed of the athlete, the force mat sends the number of contacts made within a set period of time to a laptop via bluetooth.
Some more basic pieces of equipment including scales, height measuring rail, medicine ball and sit & reach box. Attributes measured with these pieces of equipment are weight, height, upper body power and flexibility.


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How Well Do You Know Your Constitution?
July 19, 2010 Leave a comment
Elected Officials and Candidates are invited to a non-partisan two-day course on the U.S. Constitution.
The public is also welcome.
What: Discover our founders’ worldview of law and government. Obtain a working knowledge of the Declaration of Independence, the U.S. Constitution, and the Bill of Rights in this enlightening course.
Topics will include:
– the history of the United States leading to the Declaration of Independence.
– the beliefs of our Founding Fathers and their Five-Fold Formula.
– the drafting of the Constitution, the Bill of Rights, and the amendments.
After each topic there will be Q&A.
Who: Instructor: Pastor David Whitney, Senior Instructor for Institute on the Constitution.
Institute on the Constitution is an educational effort through the law office of Peroutka & Peroutka of Pasadena, MD that intends to reconnect Americans to the history of the American Republic and to their heritage of freedom under law.
When: Friday, July 30, 5:00-9:00pm [Doors open at 4:30]
& Saturday, July 31, 9:00am-9:00pm [Includes 1 hr break for dinner]
Where: 12 Carroll Street, Westminster, Maryland 21157.
Enter the side door in side parking lot (next to Carroll Street Solar).
Parking also available at Carroll Lutheran Church parking lot.
Why: Elected officials swear to uphold and defend the U.S. Constitution against all enemies – foreign and domestic. To properly uphold and defend the Constitution, we must first thoroughly understand it. Pastor Whitney says: “We can restore our Constitutional Republic only if we have a working knowledge of the Constitution, Declaration of Independence, and Bill of Rights.”
We will be happy to publicize the name of candidates and elected officials who complete this course.
Payment Options: Cost is $35
1. Pay by Credit Card– Select the desired amount of tickets in the “Quantity” field and click “Order Now” above to pay by credit card.
2. Pay by Check– Select the desired amount of tickets in the “Quantity” field and click on “Show other payment options,” then “Pay Offline” and then “Pay by Check.”
Reserve your seat early as we expect a full house. (Registration Below)
Organized by Suzanne Hill of Ron Smith Show Fans and Kathy Fuller of Carroll County Republican Women’s Club.

domain: law


13 October 2019
Sundergarh: Sending a clear message that there will be no compromise when it comes to ‘Mo Sarkar’ programme, Secretary to Chief Minister, Transformation and Initiatives (5T), VK Pandian on Sunday visited the District Headquarters Hospital, Sundergarh. And the result was that the CDMO-in-charge was suspended and a show-cause notice was issued to the Collector.
Pandian along with National Health Mission (NHM) Director Shalini Pandit and Development Commissioner Suresh Mohapatra today visited different wards of the hospital.
They began their inspection from the Mother-Child unit of the hospital. Here they interacted with admitted patients. Their next stop was the hospital pharmacy followed by other indoor wards. Pandian also visited the CT scan centre and interacted with departmental heads and other district-level officials.
Sometime later it came to fore that the Chief district Medical Officer-in-charge (CDMO) Dr Pankaj Patel has been suspended and a show-cause notice issued to the Collector Nikhil Pawan Kalyan by the State Government for lapses in implementing ‘Mo Sarkar’ initiative in the hospital.
The 5T Secretary has been touring remote districts of Odisha since last four days. The senior officials are touring Government-run healthcare institutions to get grassroots-level feedback from the beneficiaries. 'Mo Sarkar' is an initiative of the State Government to ensure transparency in governance.


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Hello, I’m using seamly in a while, so cool! but I have an issue now, for print my pattern for cutter machine they ask me to use the hpgl, so I open my svg file in inkscape and I save in hpgl. No problem for the print, but the label disappear. In the print came out the pattern and the grainline, no label? it is possible to fix this problem? thanx a lot! Paola
Hello and welcome @paolarobiolio1.
Is that the file hpgl? If so, then it could be that hpgl is a cutting file and doesn’t cut out the labels.
Hello Grace, I was thinking that but the patterns of the other user with different program came out with label! looks that some get lost in the conversion form svg seamly format in hgpl format. thanx!
thanx I fix the problem. I just need to sign when I save the pattern as sgv text as a path.
Oh, wonderful I don’t know much about cutting machines, etc. - I’m only a home sewer but I tried to help.

domain: design


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Everyone will be concerned following the tragic events at Grenfell Tower on the 14 June 2017. While there are no longer any tower blocks in our area (Dylan Thomas House on Turnpike Lane was demolished nearly 20 years ago), many will have concerns about fire safety or have family or friends living in buildings that could be a concern. Everyone has the right to feel safe in their home.
To this end, Homes for Haringey has asked that we share the following letter and link to FAQs. They have also shared the following documents that address fire safety and arranged Fire Safety drop-in sessions for those living in high-rise tower blocks. It will take time to establish what caused the disaster at Grenfell Tower and such loss of life but the immediate priority must be to be informed, stay safe, give reassurance and make sure we all stay involved.
Photo credit: Nico Hogg/Flickr
Earlier this year PMRA was awarded money by central government to […]
Yesterday's meeting A Low Traffic Future for Haringey – healthier, fairer […]
GENERAL MEETING ON 11 SEPTEMBER 2019 22 residents attended Clarendon Development […]
It's now a couple of months since St William told us […]
© Parkside Malvern Residents Association

domain: sociology