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Steven Soderbergh's 10 Most Underrated Movies Currently Available To Stream
By Olivia Armstrong Twitter @itslivarmstrong Aug 8, 2014 at 1:58pm
Photo Illustration by Jaclyn Kessel; Photos Courtesy of Everett Collection
Steven Soderbergh's latest directing endeavor, The Knick, premieres on Cinemax and Max Go tonight at 10. The Knick, a medical drama starring Clive Owen as an early 20th-Century doctor, might just be the series the summer needed. In addition to The Knick, there are plenty of underrated films from Soderbergh's career available on streaming right now. Since you're most likely familiar with his debut Sundance hit, Sex, Lies, and Videotape, and his biggest Hollywood blockbuster, Ocean's Eleven, here are ten of the director's films ranked from most to least underrated.
'King of the Hill' (1993)
This period piece follows young Aaron (Jesse Bradford) growing up hard during the Great Depression. A longtime passion project, Soderbergh had to beg, borrow, and steal to get this film made, only for it to flop at the box office. After the success of Sex, Lies, and Videotape, the young director struggled to uphold his reputation as Miramax's golden boy, torn between what he wanted to make and the films the Weinsteins wanted from him. At this point in Soderbergh's career, he and his protagonist share a similar quality of trying to be someone they're not, giving the film a deeply personal tone. See where you can stream King of the Hill on GoWatchIt.
'Schizopolis' (1997)
Experimenting for the first time with non-linear narrative structure, something Soderbergh took with him to later projects like Traffic, Schizopolis was — to put it mildly — a trip. Soderbergh stars alongside ex-wife Betsy Brantley in this three-act indie satire that came and went so quietly from the box office, it barely made a peep. Schizopolis was made during the director's lowest point in his career. Even though it bombed, it was anything but an artistic failure, as it now feels like one of his most raw, completely fearless projects of his entire filmography. See where you can watch Schizopolis on GoWatchIt.
'Gray's Anatomy' (1996)
After working with Spalding Gray on King of the Hill, Soderbergh followed the famous monologist as he struggled through his diagnosis of Macular pucker, a rare and complicated ocular disease. Soderbergh kept himself completely removed form his first feature documentary and through Gray's interviews, we not only see a man struggling with illness but also having to deal with slowly saying goodbye to his career. See where you can stream Gray's Anatomy on GoWatchIt.
'Bubble' (2005)
Purposefully featuring only nonprofessionals and filmed without a script, many thought Soderbergh had slipped back into his weird Schizopolis days with Bubble. Soderbergh experimented with a new release strategy at the time by releasing the film in theaters and on cable the same day, then on DVD later that week. Had Soderbergh not done this, it's doubtful Bubble would have seen the slow-growing following it eventually acquired. See where you can stream Bubble on GoWatchIt.
'The Limey' (1999)
Sticking with his crime theme of the late 90's and early aughts, Soderbergh plays around once again with unstructured narratives amidst complex subject matter. He uses bizarre flashback sequences that include scenes from old movies featuring Terence Stamp, who plays his main character, Wilson. Even though the film was a flop, it's a must-see if you're a Soderbergh fan and want to see wacky, experimental editing and sound design done right. See where you can stream The Limey on GoWatchIt.
'The Girlfriend Experience' (2009)
This portrait of the upper crust during the 2008 financial crisis is told through the eyes of high-end Manhattan escort, Chelsea, played by real-life porn star, Sasha Grey. Chelsea doesn't just sleep with her clients, but specializes in being a girlfriend to men who are too busy with work to be in a committed relationship. Soderbergh hired Grey to help make the premise feel as real as possible. Even though Grey's performance got mixed reviews from critics; sequences where she might be over-acting, don't feel out of place in the slightest given her job description. See where you can stream The Girlfriend Experience on GoWatchIt.
'And Everything Is Going Fine' (2010)
Soderbergh's second documentary following the life of the late Spalding Gray, who committed suicide in 2004, is a 90-minute monologue made up of various interviews with the eclectic actor. No talking heads, no photos — just archival footage and home videos of Gray discussing his childhood and career. Gray talks about how some actors are born great at what they do because they enjoy lying; although ironically enough it's unclear in the footage whether or not he's telling the truth or simply acting. See where you can stream And Everything Is Going Fine on GoWatchIt.
'Out of Sight' (1998)
Breaking out of his artistic funk, Soderbergh came back in full force with the crime-comedy Out of Sight, starring George Clooney, Jennifer Lopez, Ving Rhames, and Don Cheadle. The movie is a perfect example of how easily Soderbergh weaves through genres and filmmaking style while still keeping his signature touch and tone. By the time Out of Sight was released and Soderbergh was jogging Hollywood's memory from the days of Sex, Lies, he completed a drama, a documentary, a satire, and a crime flick. See where you can stream Out of Sight on GoWatchIt.
'Erin Brockovich' (2000)
Soderbergh was a busy man in the early aughts, churning out Hollywood blockbusters left and right and putting to rest any doubt about him within the industry. An early success was Erin Brockovich, which earned Julia Roberts her first Oscar for playing the titular single mom turned consumer advocate. The film was also nominated for Best Picture and Best Director, but Soderbergh lost the latter — to himself, for directing Traffic. See where you can stream Erin Brockovich on GoWatchIt.
'Traffic' (2000)
Perhaps his most familiar film, Traffic is Soderbergh's Oscar-winning, disjointed drug tale starring Benicio Del Toro, Michael Douglas, Catherine Zeta-Jones, and Don Cheadle. To distinguish various perspectives of the same war on drugs, Soderbergh filmed each set of characters in different tints. Del Toro's story line was filmed in the director's familiar yellow haze, while Michael Douglas' family was tinted in blue, symbolizing his daughter's heroin addiction. Though Soderbergh won the Oscar for Best Director, the film lost out to Gladiator for Best Picture. See where you can stream Traffic on GoWatchIt.
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Picasso's art closely follows his personal experiences and also reflects his views on society and politics. Even his choice of colors play an important role, with blues and greens reflecting a depressive state and pinks and oranges showing the return of love and happiness in his life.
There is a great deal that kids can learn from Picasso's work. How closely colors are related to our emotions, for example, or how art reflects not just the artist's emotional state, but the state of society as a whole. Many of Picasso's works have lots of layers and depth, but that doesn't mean that kids can't do activities based on them!! Here are 10 Pablo Picasso projects for kids to engage in!
Among the most popular of Picasso's Cubism works are his paintings featuring faces. The combination of a front and side view renders itself to some interesting craft projects for kids, like these Picasso faces tree ornaments from Kids Activities Blog. This Christmas, go arty with some really cool ornaments.
It is to Picasso's credit that he can make a simple art of two hands clasping a bouquet a grand symbol for peace and brotherhood. This lovely collage from One Project Closer is derived from Picasso's 'Bouquet of Peace' and makes use of some lovely colors!
During the early 1900's, Picasso experimented with sculptural design and made a guitar sculpture out of cardboard. It was impressive but too flimsy due to which the artist made a sturdier one later, in metal. Kids can try their hand at making the cardboard version with this easy tutorial from Make it and Love it.
The period from 1901-1904 is know as Picasso's 'Blue Period' since most of his work during this time were full of shades of green and blue. This was a depressing time for him, and he often painted sad faces and sick or starving people. Art Projects for Kids has a great way to help kids understand the emotions behind the blue period with a downloadable tutorial.
Picasso's collage painting, 'The Three Musicians' is a wonderful example of his cubist style and is said to represent the artist himself along with two of his close friends. Room 101 art showcases an adorable way to recreate this painting, with a collage, of course!
This is a great book to introduce kids to the famous artist. With kid-friendly language and lots of images, this is a must buy for your child!
Super Coloring has many printable coloring pages of artists' works, and there is one featuring Pablo Picasso's self-portrait as well! While he has created several self-portraits, this is one of the most popular, and was painted in 1907, and reflects his cubist style.
Picasso was among the first artists to use collage techniques in his art. So combine this technique with his cubism style to make these fun self-portrait collages as shown in Meri Cherry. Watch out – it can get quite addictive!
Picasso's work focused on some themes more than others, like jesters, acrobats, birds and animals. The rooster was one of his favorites and is prominent in, 'Le Coq', a work of art that reflects some lovely lines and colors. Deep Space Sparkle shows a lovely art project using oil pastels.
Just as Picasso's 'Blue Period' works reflected sadness and despair, his 'Rose Period' reflected much more cheer, with lots of orange, peach and pink. Deep Space Sparkle has a woven placemat heart in this color scheme that are really easy to make!
Show your kids pictures of Picasso's work from various periods of his life, and they'll soon begin to appreciate them. Who knows, you might be inspired to make your own Picasso project!!


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Police: Man gunned down during fight in Austin
CHICAGO (SUN TIMES MEDIA WIRE) - A man was shot to death early Wednesday during a fight in the Austin neighborhood on the West Side, police said.
The 21-year-old confronted another male at 5:17 a.m. in the 5200 block of West Gladys and, during the fight, the suspect pulled out a firearm and shot the man in the head, according to Chicago Police.
The man was pronounced dead at the scene, police said. The Cook County medical examiner's office did not immediately provide information on the fatality.
No one was in custody early Wednesday as Area North detectives conducted a homicide investigation.
3 transported from Cook County Jail to area hospitals for possible drug overdoses: CFD

redpajama_set_name: RedPajamaCommonCrawl


TEHRAN, Dec. 07 (Shana) –The National Iranian Oil Company (NIOC) and Royal Dutch Shell have signed a memorandum of understanding (MoU) to conduct studies on Azadegan, Yadavaran and Kish oilfields in Iran.
Noureddin Shahnazizadeh, managing director of the Petroleum Engineering and Development Company (PEDEC) from NIOC and Hans Nijkamp from Shell inked the deal in the presence of NIOC Managing Director Ali Kardor on Wednesday.
Based on the cooperation document, Shell will assess development projects of the fields.


text:
\section*{ }Solid planet cooling, and how it connects to volcanic-tectonic evolution, defines the Earth's thermal history. At present, the cooling of our planet's interior is associated with plate tectonics. At mid-ocean ridges, plates are created by decompression melting of mantle rock. As plates spread, they cool and transfer heat. Oceanic plates eventually subduct back into the mantle, and cold rock is mixed into the progressively cooling interior of our planet. Heat transfer associated with macroscopic motion is, by definition, thermal convection. Plate tectonics is thus a component of mantle convection and the Earth's convective cooling. Given this, a change in cooling rate (Figure 1) could reasonably be taken to indicate a change in the tectonic mode of our planet [Condie et al., 2016]. There is an alternative that does not require a change in the global tectonic mode of the Earth. The alternative hypothesis is connected to the cycling of water between Earth's interior and surface.\\

Figure 2 shows petrological constraints [Condie et al., 2016; Herzberg et al., 2010] along with a thermal history model that couples thermal convection in a planet's interior to deep water cycling [Sandu et. al., 2011]. This is one model case from thousands we have run (Figures 3 and 4). Our modeling suites account for temperature and hydration effects on mantle viscosity [Kohlstedt, 2006; Li et al, 2008], melting and volcanism that can dehydrate the mantle [Hirschmann, 2000; Katz et. al., 2003], and processes that recycle surface water to the mantle [Ulmer and Trommsdorff, 1995; Rupke et al., 2004]. Mantle de-watering occurs at mid ocean ridges and re-watering at subduction zones. The amount of water initially in the mantle is an initial condition. The fraction of water in melt that makes it to the surface, $(\chi_d)$, and the fraction of water carried into the deep mantle with subducting slabs, $(\chi_r)$, represent de- and re-watering efficiencies. Surface heat flow follows the scaling form of $Nu\sim Ra^{\beta}$, where $Nu$ is the nondimensional heat flux, $Ra$ quantifies the vigor of mantle convection, and $\beta$ is a scaling parameter that accounts for variations in plate strength affecting the motion of tectonic plates and associated mantle cooling [Conrad and Hager, 1999; Korenaga, 2003; Hoink et al., 2013]. In all cases, plate velocity parameterizations are such that model plate velocities, after 4.6 Gy of evolution, match present day values. Further model description can be found in the supplemental material.\\

\begin{figure}
  \centering
  \includegraphics[width=\linewidth]{Fig1.jpg}
  \caption{Figure 1: Petrological data from Condie et. al. [2016] along with their conceptual interpretation of the data.}
\end{figure}

The coupling between deep water cycling and thermal convection in the Earth's mantle leads to feedbacks that affect planetary evolution [Crowley et. al., 2011]. Internal temperature changes alter the nature of deep water cycling, which feeds back and alters mantle thermal evolution. If, for example, mantle temperature is relatively high, melt production can increase. Accompanying higher melt production are greater rates of mantle de-watering, leading to a stiffer mantle [Kohlstedt, 2006; Li et al, 2008] and a less efficient heat transfer. This, in turn, can act to increase mantle temperatures. Heating proceeds until temperature effects on mantle viscosity can outpace those of mantle dehydration, thereby reducing viscosity and allowing for faster convection, which acts to offset the heating effect associated with dehydration. Recycling water into the Earth's interior is also associated with potential feedbacks. For cooler conditions, hydrated mineral phases are stable to greater depth, [Ulmer and Trommsdorff, 1995; Rupke et al., 2004] and as a result, the ability to cycle water into the interior can increase with mantle cooling. Water cycled into the mantle lowers mantle viscosity, which decreases the resistance to plate overturn and, by association, increases mantle cooling. The strength of these coupled feedbacks evolve through time, and this opens the potential of a wider diversity of thermal histories as compared to a situation without deep water cycling. \\

The model of Figure 2 started warm, contained 1.5 present day ocean mass equivalents (OM) of water in the mantle and evolved as water cycled between the surface and interior. The evolution consisted of three phases: rapid initial cooling, near constant temperature, and a steady decrease to present day. The first phase was facilitated by a hot and hydrated mantle. These factors decrease mantle viscosity which increased convective vigor and mantle cooling. The second phase is highlighted by a flattening of the cooling curve consistent with the data of Condie et al. [2016]. The data of Herzberg et al. [2010] is associated with warmer temperatures but overall trends are similar. Mantle degassing continued beyond the initial rapid phase of mantle cooling. Continued mantle dehydration drove an increase in viscosity which damped the efficiency of heat transport. Decreased heat transport drove an increase in mantle temperature which offset the tendency for the mantle temperature to drop as internal heat sources decayed. This occurred to the point where there was a near balance between the two effects which lead to a flat line cooling phase. The flat line behavior correlated with a model water evolution phase during which surface water mass increased due to the dominance of outgassing from the interior (Figure 2b). Over time, the rate of mantle dehyrdration waned and could not maintain a flat line trend. As the mantle cooled, lithospheric plates thickened and the stability field for hydrated minerals deepened allowing a larger capacity of water rich rock to be transported back into the deep mantle (subduction zones transitioned from being dry to wet). At $\sim$2.0 Gyr of model time, mantle de- and re-hyrdration became comparable which terminated the flat line cooling phase. The final phase was characterized by internal temperature tracking the decay of radiogenic heat sources in the mantle. For a number of cases explored, rehydration exceeded mantle dehydration which lead to a steeper final cooling phase. \\

\begin{figure}[b!]
  \includegraphics[width=\linewidth]{Fig2.jpg}
  \caption*{Figure 2: Representative thermal evolution with deep water cycling effects compared to petrologic data (a). The blue curve is the thermal evolution model. The red and black dots are data from Condie et. al. [2016] and Herzberg et. al. [2010]. (b) Model surface water evolution. }
  \label{fig:appfig1}
\end{figure}

\begin{figure*}[t]
  \includegraphics[width=\linewidth]{Fig3.jpg}
  \caption*{Figure 3: Four panels representing the final mantle potential temperature (a), the onset time of the most recent phase of mantle cooling (b), the mantle temperature after 1.5 Gy of model evolution (c), and the present day Urey ratio (d).  }
  \label{fig:appfig1}
\end{figure*}

Figure 2 plots an illustrative case from a large number of models that were run over varied model assumptions, parameter values, and initial conditions. In Figure 3, each open circle represents the result of one model for a distinct combination of initial conditions and parameter values. The four plots represent the final mantle temperature, the age at which the most recent cooling phase initiated, the mantle temperature after 1.5 Gy of model evolution, and the present day ratio of mantle heat sources to mantle heat loss (referred to as the mantle Urey ratio). The Urey ratio values account for the effects of present day continental area [Grigne et al., 2001; Lenardic et al., 2011]. There are six column sets of model cases for each value of $\beta$. Decreasing $\beta$, from left to right, parameterizes the effects of plate strength progressively offering enhanced resistance to plate motion [Conrad and Hager, 1999]. The three red column sets, for each fixed $\beta$ suite, represent an initial mantle heat source density that is chondritic [e.g., Schubert et al., 1980] while the blue sets represent reduced mantle heat source density [Jackson and Jellinek, 2013]. The three different columns, for each fixed $\beta$ and heat source density sub-suite, represent increasing initial thermal conditions (from right to left columns, the starting temperature is 900 K, 1600 K, and 2300 degrees). Each individual model set column uses the results of 128 cases that varied initial water volume along with de- and re-gassing parameters. Initial water volumes ranged from 0.1 to 6 ocean mass equivalents. Re- and de-gassing efficiency parameters spanned the high to low parameter ranges from Sandu et al. [2011]. \\

Figure 3 demonstrates the diversity of model behavior associated with feedbacks between deep water cycling and thermo-tectonic evolution. Differing combinations of de- and re-watering efficiencies, together with variable thermal parameters and initial conditions, can produce a range of thermal histories. The green transparent rectangles in Figure 3 delineate the range of model cases that are consistent with data constraints. Petrological data provide a constraint for onset time of the Earth's most recent cooling phase and mantle potential temperatures in the flat line cooling phase. Although the absolutes for different petrologic data sets are not in exact agreement, the trends match reasonably well (figure 2a). In particular, both data sets indicate that from the onset of the most recent cooling phase to the present day, the mantle has cooled by 100-200 $^o$C. Another constraint on thermal evolution is the present day Urey ratio (Ur) which, within data uncertainty, is between 0.2 and 0.5 [Jaupart et al., 2007]. \\

Grouping model results into variable $\beta$ sets reflects the fact that different values of  $\beta$ are associated with different hypothesis regarding solid planet dynamics. A model with $\beta=0.33$ is based on the hypothesis that the dominant resistance to the motion of tectonic plates comes from interior mantle viscosity [Davies 1980; Schubert et al., 1980]. A model that with $\beta=0$ is based on the hypothesis that the dominant resistance to the motion of tectonic plates comes from the strength of plates themselves with any changes in internal mantle viscosity having no effect on plate velocity [Christensen, 1984; 1985]. Intermediate values reflect variable hypotheses regarding the balance between internal mantle and plate sourced resistance to plate motion [Conrad and Hager, 1999]. Our modeling strategy follows that of McNamara and VanKeken [2000]: running a large number of models, under varied assumptions, allows different hypotheses to be assessed against each other in a statistical manner. It is no surprise, given parameter and initial condition uncertainties, that cases can be found that match data constraints from models that are based on fundamentally different physical assumptions. Given this, a probabilistic approach becomes necessary to: 1) determine if the ability of any hypothesis to match data is statistically meaningful (that is, to determine if model results, that match data, may be outliers in parameter space), and 2) to discriminate between competing hypothesis. \\

The Urey ratio has come to be seen as a key value that can be used to discriminate between competing thermal evolution hypotheses [Conrad and Hager, 1999; Korenaga, 2003; Jaupart et al., 2007]. Model Urey ratio values (Figure 3d) can be viewed probabilistically as in Figure 4. Model output distribution, when all $\beta$ cases are plotted together, is not uni-modal. The model Ur peak at $\sim$0.6 is close to that obtained by first generation thermal history models that did not account for deep water cycling and/or the effects of strong plates resisting motion [Davies 1980; Schubert et al., 1980]. The peak at $\sim$0.35  is more in line with data constraints [Jaupart et al., 2007]. \\

\begin{figure*}
  \includegraphics[width=\linewidth]{Fig4a.jpg}
  \includegraphics[width=\linewidth]{fig4b2_LQHT.jpg}
  \caption*{Figure 4: Distribution of present day Urey ratios. The top set of panels is for cases with chordritic heat sources [e.g., Schubert et al., 1980]. The bottom set is for cases with reduced mantle heat source density [Jackson and Jellinek, 2013]. The large plot at the left, for the upper and lower sets, shows results for all $\beta$ values. The smaller plots to the right of each large plot show the individual $\beta$ value distributions.}
  \label{fig:appfig1}
\end{figure*}

Including deep water cycling into classic thermal history models that do not include the effects of strong plates can lower Urey ratio values to a point such that the data constraints can be matched. This was already noted by Sandu et al. [2011]. A probabilistic approach, which covers larger parameter space allowing distribution functions to be constructed, shows that although this conclusion is valid, the model distribution peak is located outside the data window (Figure 4, top panels). Non-classical assumptions regarding initial heat source density can bring the distribution peak within the data window (Figure 4, bottom panel). None the less, models that allow plate strength to provide a component of resistance to plate motion are statistically preferred as they bring the distribution peak deeper into the data window (Figure 4, smaller panels). As $\beta$ decreases, the model Ur distribution peak shifts towards lower values. When $\beta$ is equal to 0.20, the model distribution becomes uni-modal with a peak Urey ratio of $\sim$0.35 (Figure 4). However, there is a limit to this behavior. As $\beta$ is lowered towards zero, model output looses a uni-modal character and spans a wider Urey ratio range. \\

Shifting $\beta$ towards zero means that plate velocities progressively do not scale with convective vigor and as such, become constant over the full evolution time. Any enhanced cooling potential, due to enhanced subduction under hotter mantle conditions, is thus damped. This weakens a negative, i.e., buffering, feedback within the system. Weakening this negative feedback means that final model results become more sensitive to initial conditions [Korenaga, 2016]. If the negative feedback is removed altogether, $\beta \leq 0$, then the model system has no stable attracting state and results become highly sensitive to assumed initial conditions and the effects of parameter uncertainties become large [Moore and Lenardic, 2015]. This is reflected in Figure 4  for the lowest $\beta$ suites which are characterized by model outputs with a multi-modal distribution. Removing a thermal feedback also alters water cycling. Cooler conditions allow for enhanced water cycling into the mantle (water cycling into the mantle is also a cooling feedback as it lowers viscosity which allows for enhanced convective overturn and heat loss). The lack of a subduction cooling feedback can move the system towards one that is dominated by mantle de-watering over larger portions of model evolution. Thus, de-watering can outweigh re-watering over a larger portion of potential parameter space. This tends to shift cooling times closer toward present day and can also lead to model distributions that allow for higher Urey ratio values [Crowley et al., 2011]. \\

Many of the model cases explored do not match observational constraints for the Earth. However, the range of potential solutions that can match data constraints, given uncertainties in the data, initial conditions, model parameter values, and variable hypotheses regarding the role of plate strength, is significant (the percentage breakdown of models that can match data constraints is provided in the supplemental material). A very low $\beta$ hypothesis is associated with an extreme sensitivity to parameter uncertainty. In addition, the lowest $\beta$ cases all run too hot relative to data constraints (Figure 3). Collectively, this makes a low $\beta$ hypothesis statistically weak and cases with a $\beta$ range between 0.33-0.20 are favored. Within that model range, an initial heat source distribution lower than chondritic is also favored, whereas very cool starting conditions are not. Of the models subject to those statistical preferences, 13.3 percent match data constraints (the total number of models in that subset still exceeds 1000 cases). That is to say, solutions of the type shown in Figure 2 are not outliers. From this statistical perspective, petrologic data trends can be accounted for if deep water cycling and strong subduction zones are considered in tandem. Subduction zones that are so strong that they provide the dominant resistance to plate motion are not statistically preferred (that is, mantle viscosity remains an important variable for determining plate velocities). A change in tectonic regime is not required to account for the petrologic data trends. \\

There are added model implications that can provide enhanced layers of hypothesis testing. The cases from our modeling suite, that can match thermal constraints, suggest a change in the balance of mantle de- and re-watering at 2.0-2.5 Gya as subduction zones became cool enough to recycle a level of water that could keep pace with or outweigh mantle de-watering. This implies a switch from relatively dry to wet subduction, here caused by a thickening of the hydrated layer in subducting plates as the Earth cooled. An increase in water volume entering into the mantle at subduction zones can result in the production of felsic rather than mafic crust. As the amount of Earth's surface area covered by felsic crust increases, its oxidative efficiency decreases, leading to a rise in atmospheric O$_2$ [Lee et al., 2016]. A rise in atmospheric O$_2$ should then be coincident with the onset of the Earth's most recent cooling phase as constrained by petrological data [Condie et al., 2016; Herzberg et al., 2010]. Available data constraints [Lee et. al., 2016] are consistent with this model implication.  \\

In order for our models to match present day Urey ratio values, mantle re-watering needs to be in balance with or exceed de-watering from the termination of a flat line cooling phase to the present day (i.e., from 2.0 Gya to the present). Models in which re-watering is exceeding mantle de-watering over this time scale lead to lower Urey ratio values [Crowley, 2011] putting them deeper into the allowable data constraint range from Jaupart et al. [2007]. The balance of mantle de-watering and re-watering over geologic time is difficult to constrain. Efforts to do so do, however, suggest that mantle re-watering has exceeded de-watering over the last 500-600 Million years [Rupke et al., 2004; Parai and Mukhopadhyay, 2012]. This is consistent with the water balance  implications from our model cases that can match thermal history constraints. \\

As a final word, we offer a caution on extrapolating our results to other terrestrial planets. Although observations can constrain the range of viable model solutions for the Earth's thermal evolution, this does not mean that the same range needs to hold for terrestrial planets in general - be they planets in this solar system or in others. Theoretical models applied over geologic time frames need to effectively tune a range of parameter uncertainties by using Earth constraints. Model cases that fall out of the Earth viable range are not considered physically implausible. They are, instead, potential model paths for a terrestrial planet's evolution that are not in line with constraints on the evolution of a particular terrestrial planet (Earth). Thermo-tectonic history models have been and continue to be extrapolated to terrestrial planets orbiting stars other that our own. Often this is done by adjusting only a few variables, e.g., planetary size, while leaving others constant. The diversity of solutions for models that couple water cycling to planetary thermal evolution (Figures 3 and 4) highlight a deficiency in this approach and argue for a shift toward a fully statistical/probabalistic approach that does not hinge on Earth tuned results. \\

\section*{References}

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Conrad, C. and Hager, B., 1999, The thermal evolution of an earth with strong subduction zones, Geophysical Research Letters, 26, 3041-3044. \\

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Korenaga, J., 2003, Energetics of mantle convection and the fate of fossil heat, Geophysical Research Letters, 30, 1437-1440. \\

\noindent
Korenaga, J., 2016, Can mantle convection be self-regulated?, Sci. Adv., 2016, 2:e1601168. \\

\noindent
Lee, C. A., Yeung, L. A., McKenzie, N. R., Yokoyama, Y., Ozaki, K. and Lenardic, A., 2016, Two-step rise of atmospheric oxygen linked to the growth of continents, Nat. Geosci., 9, 417-424.   \\

\noindent
Li, Z.-X. A., Lee, C.-T. A., Peslier, A.H., Lenardic, A. and Mackwell, S.J., 2008, Water contents in mantle xenoliths from the Colorado Plateau and vicinity: Implications for the mantle rheology and hydration-induced thinning of continental lithosphere, J. Geophys. Res., 113, B09210. \\

\noindent
McNamara, A. K., and P. E. van Keken (2000), Cooling of the Earth: A parameterized convection study of whole versuslayered models, Geochem. Geophys. Geosyst., 1, 1027, doi:10.1029/2000GC000045. \\

\noindent
Moore, W.B., and A. Lenardic, 2015, The efficiency of plate tectonics and non-equilibrium dynamic evolution of planetary mantles, Geophys. Res. Lett.,42, doi:10.1002/2015GL065621, 2015. \\

\noindent
Parai, R., and Mukhopadhyay, S., 2012, Water in the oceanic upper mantle: Implications for rheology, melt extraction and the evolution of the litho- sphere, Earth Planet. Sci. Lett., 317-318, 396–406. \\

\noindent
Rupke, L. H., J. P. Morgan, M. Hort, and J. A. D. Connolly, 2004, Serpen- tine and the subduction zone water cycle, Earth Planet. Sci. Lett., 223, 17–34, doi:10.1016/j.epsl.2004.04.018. \\

\noindent
Sandu, C., Lenardic, A. and McGovern, P.J., 2011, The effects of deep water cycling on planetary thermal evolution, Journal of Geophysical Research, 116, B12404. \\

\noindent
Schubert, G., Stevenson, D., Cassen, P., 1980. Whole planet cooling and the radiogenic heat source contents of the earth and moon. J. Geophys. Res. 85, 2531–2538. \\

\noindent
Ulmer, P., and V. Trommsdorff, 1995, Serpentine stability to mantle depths and subduction-related magmatism, Science, 268(5212), 858–861, doi:10.1126/science.268.5212.858.

\clearpage

\newpage

\section{Appendix: Methods}

\subsection{Convection}
\indent Here we use the one-dimensional energy equation [Schubert et. al., 1979; Schubert et. al., 1980] to obtain the time rate of change of the Earth's average mantle temperature ($\dot{T}$)
\begin{equation} \label{PT_energy_balance}
\rho CV\dot{T} = -3 Aq_m + VQ(t)
\end{equation}
where $\rho$ is mantle density, $C$ is mantle heat capacity, and $q_m$ is the mantle surface heat flux. Mantle volume, $V$ and surface area $A$ are calculated as $R_m^3-R_c^3$ and $R_m^2-R_c^2$, respectively, where $R_m$ is the radius of the mantle and $R_c$ is the radius of the core. In this equation $T$ is the spherically averaged mantle temperature sense. In (\ref{PT_energy_balance}) it is assumed that the system is internally heated with an insulating bottom boundary. Heat is produced by radiogenic decay according to
\begin{equation} \label{heat_src}
Q(t) = Q_0e^{-\lambda t}
\end{equation}
where $Q_0$ and $\lambda$ are constants and $t$ is the current time.\\
\indent The Urey ratio $(Ur)$, which defines the ratio of heat produced within to heat transferred through the mantle surface, is defined as
\begin{equation} \label{Ur}
Ur = \frac{VQ}{Aq_m}.
\end{equation}
When $Ur>1$, the planetary mantle is heating up. Alternatively, a value of $Ur<1$ means heat flow out of the mantle exceeds heat generated within the mantle and thus the mantle cools. \\
\indent The Rayleigh number $\left(Ra\right)$, a ratio of forces driving convection to those resisting it, is defined as
\begin{equation} \label{Ra}
Ra = \frac{g\alpha \Delta TZ^3}{\eta\kappa}
\end{equation}
where $g$, $\alpha$, $Z$, $\eta$ and $\kappa$ are gravity, thermal expansivity, depth of the convecting layer, kinematic viscosity and thermal diffusivity, respectively. The value $\Delta T$ is the temperature difference driving convection defined as $T - T_s$, the difference between the mantle and surface temperatures. The relationship between a nondimensional heat flux ($Nu$) and $Ra$, which takes the form
\begin{equation} \label{Nu}
Nu = \frac{q_mZ}{k\Delta T} = \left(\frac{Ra}{Ra_{cr}}\right)^\beta
\end{equation}
is used to solve for $q_m$, where $k$ is thermal diffusivity, $Ra_{cr}$ is the critical Rayleigh number which determines the onset of convection and $\beta$ is a scaling exponent. The value of $\beta$ for classic thermal history models is assumed to be 1/3 [Turcotte et. al., 1967; Solomatov 1995]. This assumes a plate tectonics mode of behavior in which the dominant resistance to plate motion comes from mantle viscosity. Lower values are also considered to mimic the effects of enhanced resistance coming from the strength of plates and/or plate margins [Christensen, 1985; Conrad and Hager, 1999; Korenaga, 2008]. \\
\indent A velocity scale $(u_c)$ is needed to compute degassing and regassing of the mantle. Fourier's law is rearranged to determine the lithospheric thickness according to the equation
\begin{equation} \label{Db}
D_b = k\frac{\left(T_b - T_s\right)}{q_m}
\end{equation}
where \emph{k} is thermal conductivity. The temperature $T_b$ represents the temperature at the base of the lithosphere and is equivalent to $T_m$. We use boundary layer theory [Schubert et. al., 2001] to derive a boundary layer breakaway time associated with subduction of the lithosphere according to
\begin{equation} \label{ts}
t_s = \frac{1}{5.38\kappa_m}D_b^2
\end{equation}
From here, an equation for convective velocity is expressed as
\begin{equation} \label{uc}
u_c = \frac{\left(R_m - R_c\right)}{t_s}.
\end{equation}
The convective velocity scaling is of the form of $u_c \sim Ra^{2\beta}$, or more fully
\begin{equation} \label{uc_Ra}
u_c = \frac{a_1\kappa}{2\left(R_m-R_c\right)}\left(\frac{Ra}{Ra_{crit}}\right)^{2\beta}
\end{equation}
where $a_1$ is a scaling parameter. It has a value  of 5.38 for the classic case of $\beta = 1/3$ [Schubert et. al., 1979; Schubert et. al., 1980]. As can be seen in (\ref{uc_Ra}), velocity has a power dependence on $\beta$. In the endmember case that $\beta = 0$, a constant velocity would be maintained. That is to say that for any value of $Ra$, the velocity will not change. To account for variable $\beta$, in a manner that allows all model to match present day plate velocities, a velocity scale must be set. To set this scale, we  use the present day values of convective vigor and velocity, $Ra_{now}$ and $u_{now}$, respectively, with the $\beta = 1/3$  scaling used as a reference. This leads to
\begin{align}
u_{now} &= a_1\frac{\kappa}{2\left(R_m-R_c\right)}\left(\frac{Ra_{now}}{Ra_{crit}}\right)^{\frac{2}{3}} \\
u_{now} &= a_2\frac{\kappa}{2\left(R_m-R_c\right)}\left(\frac{Ra_{now}}{Ra_{crit}}\right)^{2\beta} \\
a_2 &= a_1Ra_{crit}^{2\beta-\frac{2}{3}}Ra_{now}^{\frac{2}{3}-2\beta}
\end{align}
This value of $a_2$ can be computed for each $\beta$ and provide calibrated velocity scalings that will result in comparable present day velocity for model suites with variable $\beta$ values.

\subsection{Volatile Cycling}
\indent Volatile cycling between the interior and surface has a direct influence on thermal evolution. The calculation of volatile cycling follows Sandu et. al. [2011]. Water leaves the mantle as an incompatible element participating in the batch melting process, which only occurs at mid-ocean ridges in our simplified model. Water is returned to the mantle via subduction processes.\\

To track mantle melting, the average mantle temperature calculated from (\ref{PT_energy_balance}) is converted to a temperature versus depth profile consisting of two parts: the conductive, lithospheric profile and the adiabat from the convecting mantle. The near surface temperature gradient is defined by the temperature at the surface and heat flux at the base of the lithosphere by
\begin{equation} \label{Lith_temp}
T(z)|_{z\leq D_b} = T_s + \frac{q_m}{k}z.
\end{equation}
The adiabat contribution to the thermal profile is calcuated by converting the average mantle temperature to a potential temperature and projecting to depth according to
\begin{equation} \label{adiabatic_temp}
T(z)|_{z>D_b} = T_p + \frac{g\alpha T_m}{C_p}z.
\end{equation}
Although a depth dependent temperature profile is being calculated, it does not influence the convective dynamics. \\
\indent The thermal profile is compared to a solidus to compute the amount of melt generated by upwelling mantle. Two second-order polynomial functions are used to track melt fraction [Hirschman, 2000]. The solidus defines the temperature depth profile below which all mantle material will remain in its solid phase. As temperature warms beyond the solidus, a greater fraction of the mantle will melt until the liquidus, the temperature at which the entire mantle parcel becomes melted, is reached. In the case of hydrous melting, these functions take the form
\begin{equation} \label{Solidus}
T_{sol-hydr} = T_{sol-dry}-\Delta T_{H_20}
\end{equation}
\begin{equation} \label{liquidus}
T_{liq-hydr} = T_{liq-dry}-\Delta T_{H_20}
\end{equation}
where $T_{sol-dry}$, $T_{liq-dry}$, $T_{sol-hydr}$ and $T_{liq-hydr}$ are the dry solidus and liquidus and hydrated soldus and liquidus, respectively. The last term of both equations is the temperature shift  of each curve brought on by consideration of hydrous melting. This adjustment temperature scales with water concentration in the melt according to
\begin{equation} \label{dT_H2O}
\Delta T_{H_20} = KX_{melt}^\gamma
\end{equation}
where $K$ and $\gamma$ are constants which were calibrated by Katz et. al. [2003]. The parameter $X_{melt}$ is the ratio of water in the melt fraction expressed in kg of water per kg of melt and is calculated as
\begin{equation} \label{X_melt}
X_{melt} = \frac{C_{mv}}{D_{H_2O}+F_{melt}\left(1-D_{H_2O}\right)}
\end{equation}
where $C_{mv}$, $D_{H_2O}$ and $F_{melt}$ are the bulk water composition in the solid mantle expressed as a weight fraction, the bulk distribution coefficient which takes the value of 0.01 -- highlighting it behaves as an incompatible trace element -- and the degree of melting expressed as melt fraction, respectively. The melt fraction is parameterized in power-law form as
\begin{equation} \label{F_melt}
F_{melt} = \frac{T-\left(T_{sol-dry}-\Delta T_{H_2O}\left(X_{melt}\right)\right)}{T_{liq-dry}-T_{sol-dry}}^\beta .
\end{equation}
This definition of $F_{melt}$ is valid from the surface to a depth of 300 km as constrained by observation and melting experiments. The values of melt fraction and water concentration were integrated over the melt zone thickness to provide an average to be used in the water budget calculation. \\

\begin{table*}[t!]
\caption{Model Parameters}
\centering
\begin{tabular}{l c c c}
\hline \\
Parameter Name & Symbol & Value & Unites \\ [0.5ex]
\hline \\
Initial mantle temperature & $T_{mi}$ & 1300, 2300, 3300 & K \\
Initial surface temperature & $T_{si}$ & 300 & K \\
\\
Initial radioactive heat & $Q_{mi}$ & 4.51, 3.157 & J/(m$^3$yr) \\
Radioactive decay constant & $\lambda$ & 3.4*10$^{-10}$ & yr$^{-1}$ \\
\\
Lower mantle boundary (Earth) & $R_c$ & 3471 & km \\
Upper mantle boundary (Earth) & $R_m$ & 6271 & km \\
Initial lithospheric thickness & $Z_{lith}$ & 0 & km \\
\\
Mantle density & $\rho$ & 3000 & kg/m$^3$ \\
Thermal conductivity & $k$ & 4.2 & W/(m*K) \\
Specific heat & $C_p$ & 1400 & J/(kg*K) \\
Coefficient of thermal expansion & $\alpha$ & 3*10$^{-5}$ & K$^{-1}$ \\
\\
Viscosity constant & $\eta_0$ & 1.7*10$^{17}$ & Pa*s \\
Viscosity material constant & $Acre$ & 90 & MPa$^{-r}$/s \\
Viscosity exponent constant & $r$ & 1.2 & - \\
Activation energy for creep & $AE_c$ & 4.8*$^5$ & J/mol \\
\\
Degassing efficiency factor & $\chi_d$ & 0.002, 0.02, 0.04, 0.4 & - \\
Regassing efficiency factor & $\chi_r$ & 0.001, 0.003, 0.01, 0.1 & - \\
Initial Mantle Ocean Masses & $OM_i$ & 0.1, 0.25, 0.5, 0.75, 1, 2, 4, 6 & - \\
\\
Fraction of volatile in basalt & $f_{bas}$ & 0.03 & - \\
Density of basalt & $\rho_{basalt}$ & 2950 & kg/m$^3$ \\
Average thickness of basalt & $Z_{basalt}$ & 5000 & m \\
\\
Critical Rayleigh number & $Ra_{crit}$ & 1100 & - \\
Nusselt-Rayleigh scaling parameter & $\beta$ & 0.1, 0.15, 0.2, 0.25, 0.3, 0.33 & - \\
[1ex]
\hline
\end{tabular}
\label{table:Params}
\end{table*}

\indent The melt zone thickness is dependent upon the relative positioning of the thermal profile and the solidus. The lower boundary of the melt zone is defined where a parcel of upwelling mantle reaches a temperature hot enough to begin producing partial melt. This depth will be identified by the intersection between the mantle thermal profile and solidus. The upper bound of the melt zone is defined by the near surface intersection of the solidus and thermal profile. At this depth, the upwelling mantle has cooled enough such that no more melt is being produced. The depth difference between these two cross over points defines the thickness of the mantle undergoing partial melting and contributes to the mantle degassing calculation. \\

Water is degassed at mid-ocean ridges (MOR). The rate at which water is degassed depends on the volume of mantle transiting the melt zone below the ridge, the amount of melt produces, what fraction of that melt is water and how much of that water makes it to the surface. In equation form, the degassing rate ($r_{MOR}$) is
\begin{equation} \label{rMOR}
r_{MOR} = \rho_mF_{melt}X_{melt}D_{melt}S\chi_d
\end{equation}
where $F_{melt}$ is the integrated melt fraction in the melt zone and $\chi_d$ is the degassing efficiency factor. Both $D_{melt}$ and $X_{melt}$ are calculated according to the parameterization of Katz et. al. [2003]. The areal spreading rate, $S$, is derived from a boundary layer model [Schubert et. al., 2001] and is represented as
\begin{equation} \label{areal_spreading}
S = 2L_{ridge}u_c
\end{equation}
which assumes symmetrical spreading along a constant length of ridge, $L_{ridge}$. Velocity, $u_c$, is solved within the model according to equation (\ref{uc}).\\

Water is assumed to be returned to the mantle at subduction zones. This water is bound in the serpentinized and thin sedimentary layers of the slab [Rupke et. al., 2004]. Since most water held in the sedimentary layer is lost back to the surface, the serpentinized layer is the more important factor in our calculation. The rate at which water is subducted back into the mantle ($r_{SUB}$) is
\begin{equation} \label{rSUB}
r_{SUB} = f_h\rho D_{hydr}S\chi_r,
\end{equation}
where $f_h$, $D_{hydr}$, and $\chi_r$ are the mass fraction of volatiles in the serpentinized layer, thickness of the serpentinized layer and regassing efficiency factor, respectively. In this case, $D_{hydr}$ is defined as the depth of the 700$^o$C isotherm as the hydrous phase of serpentine decomposes around this temperature [Ulmer  and Trommsdorff, 1995]. \\

Individually, equations (\ref{rMOR}) and (\ref{rSUB}) tell what is occurring independently. The overall flow rate of mantle water ($r_{Mmv}$) is
\begin{equation} \label{water_balance}
r_{Mmv} = r_{SUB}-r_{MOR}.
\end{equation}
This tracks the balance of water between the interior and surface reservoirs. When $r_{Mmv}$ is positive, the mantle is being replenished with water. When it is negative, the mantle is losing water. If $r_{Mmv}$ is zero, there is a balance between the two and the mass of water in each reservoir remains constant.

\subsection{Viscosity}
\indent The temperature dependence of mantle viscosity takes the Arrenhius form
\begin{equation} \label{nv_visc}
\eta = \eta_0exp\left(\frac{A}{RT_m}\right)
\end{equation}
where $\eta_0$, $A$, $R$ are a reference viscosity, activation energy for creep  (Weertman and Weertman, 1975) and the universal gas constant. \\
\indent Experiments have shown hydration effects have a power law effect on mantle viscosity [Carter et. al., 1970; Chopra and Paterson, 1984; Mackwell et. al., 1985; Karato and Wu, 1993] The power law was further refined to include dependence on water fugacity in olivine [Hirth and Kohlstedt, 1996; Mei and Kohlstedt, 2000]. Assuming Newtonian behavior and an empirical relation for water fugacity based on concentrations [Li et. al., 2008], the effective viscosity is given by
\begin{align} \label{vd_visc}
\eta_{eff} &= \frac{\tau}{\dot{\epsilon}} = \eta_0 A_{cre}^{-1}\left(exp\left(c_0 + c_1 ln C_{OH} + c_2 ln^2 C_{OH} \right. \right. \nonumber \\
&\left. \left. + c_3ln^3 C_{OH}\right)\right)^{-r} exp\left(\frac{A}{RT}\right)
\end{align}
where $\tau$, $\dot{\epsilon}$ are stress and strain rate. Experimentally determined constants from Li et al. [2008] are $c_0$, $c_1$, $c_2$ and $c_3$ and $C_{OH}$ is the water concentration expressed as $H/10^6$ Si. Here $\eta_0$ and $A_{cre}$ are a calibration and material constant.

\section{Appendix: Model Output Statistics}

\begin{figure}[b!]
  \centering
  \includegraphics[width=\linewidth]{OMs_logY_all.eps}
  \caption{Each open circle represents the final present day amount of water at the Earth's surface for a specific combinations of parameters and initial conditions. The final distribution of water is sensitive to the assumed initial amount of water in the system. This initial condition sensitivity made the final water distribution a weak discriminate between different model hypotheses. That is, changes in the assumed initial water volume allowed the full range of model hypothesis to match final surface water distribution with a weak statistical preference between hypotheses.}
\end{figure}

\begin{table*}[t!]
\caption{Number of Models Successfully Constrained}
\centering
\begin{tabular}{c|cccccc|c}
\hline
 & $\beta=0.33$ & $\beta=0.3$ & $\beta=0.25$ & $\beta=0.2$ & $\beta=0.15$ & $\beta=0.1$ &  \\
\hline
LQLT & 0  & 0  & 0  & 0 & 0 & 0 & 0 \\
LQMT & 41 & 29 & 16 & 5 & 0 & 0 & 91 \\
LQHT & 35 & 3  & 7  & 0 & 0 & 0 & 45 \\
HQLT & 0  & 5  & 0  & 3 & 0 & 0 & 8 \\
HQMT & 0  & 3  & 10 & 0 & 0 & 0 & 13 \\
HQHT & 2  & 3  & 10 & 0 & 0 & 0 & 15 \\
\hline
     & 78 & 43 & 43 & 8 & 0 & 0 & 172 \\
\hline

\end{tabular}
\end{table*}

Table 1 shows the range of model parameters, and Table 2 shows the models that can match data constraints broken into model subsets by variable $\beta$, initial heat source density, and initial temperatures. Of all the model cases, 3.7 percent can match data constraints. None of the cases with a $\beta$ value below 0.2 can match all the constraints. Once those cases are removed, 5.6 percent of the remaining cases can match data constraints. Statistically, models with initial heat source densities lower than chondritic [Jackson and Jellinek, 2013] are preferred. Once the higher heat source density cases are removed, 8.9 percent of the remaining cases can match data constraints. Once the coolest initial condition cases, which are not statistically preferred, are removed, 13.3 percent of the remaining cases can match data constraints. The number of cases within that reduced set is 1024. Model cases with low initial mantle water have a statistically lower chance of allowing for a mantle dewatering effect that can drive a flat line cooling phase and associated delayed mantle cooling (Figure 2). If models are further limitted to an initial mantle water content of at least one ocean mass equivalent, then 19.14 percent of the remaining models (512 total) can match data constraints.

Figure 5 shows final water distributions. The sensativity of final surface water on assumed initial mantle water volume made this a weak descriminate between different model hypotheses. It should be further noted that the surface water in our models represents water that is degassed from the mantle. Late stage water delivery could alter the final surface volume of water without having a significant effect on our thermal evolution models provided the initial mantle water is not significantly lower than one ocean mass (it was only the lower initial mantle water cases that allowed mantle re-watering to be limitted due to the lack of surface water). This further weakens the use of the final surface water as a constraint that can descriminate between competing hypothesis regarding thermal evolution.

\section*{Appendix: References}

\noindent
Carter, N.L., and Ave'Lallemant, H.G., 1970, High temperature flow of dunite and peridotite, Geol. Soc. Am. Bull., 81, 2181–2202. \\

\noindent
Chopra, P. N., and M. S. Paterson (1984), The role of water in the deformation of dunite, J. Geophys. Res., 89, 7861–7876. \\

\noindent
Christensen, U., 1985, Thermal evolution models for the earth, Journal of Geophysical Research, 90, 2995-3007. \\

\noindent
Conrad, C. and Hager, B., 1999, The thermal evolution of an earth with strong subduction zones, Geophysical Research Letters, 26, 3041-3044. \\

\noindent
Hirschmann, M. M., 2006, Water, melting, and the deep Earth H2O cycle, Annu. Rev. Earth Planet. Sci., 34, 629–653. \\

\noindent
Hirth, G., and Kohlstedt, D.L., 1996, Water in the oceanic upper mantle: Implications for rheology, melt extraction and the evolution of the litho- sphere, Earth Planet. Sci. Lett., 144, 93–108. \\

\noindent
Karato, S., and Wu, P., 1993, Rheology of the upper mantle: A synthesis, Science, 260, 771–778. \\

\noindent
Katz, R.F., Spiegelman, M. and Langmuir, C.H., 2003, A new parameter- ization of hydrous mantle melting, Geochem. Geophys. Geosyst., 4(9), 1073. \\

\noindent
Korenaga, J., 2008, Urey ratio and the structure and evolution of earth's mantle, Reviews of geophysics, 46. \\

\noindent
Li, Z.-X. A., Lee, C.-T. A., Peslier, A.H., Lenardic, A. and Mackwell, S.J., 2008, Water contents in mantle xenoliths from the Colorado Plateau and vicinity: Implications for the mantle rheology and hydration-induced thinning of continental lithosphere, J. Geophys. Res., 113, B09210. \\

\noindent
Mackwell, S.J., Kohlstedt, D.L. and Paterson, M.S., 1985, The role of water in the deformation of olivine single crystals, J. Geophys. Res., 90, 11319–11333. \\

\noindent
Mei, S., and D. L. Kohlstedt, 2000, Influence of water on plastic deformation of olivine aggregates 2. Dislocation creep regime, J. Geophys. Res., 105, 21,471–21,481. \\

\noindent
Rupke, L.H., Morgan, J.P., Hort, M. and Connolly, J.A.D., 2004, Serpentine and the subduction zone water cycle, Earth Planet. Sci. Lett., 223, 17–34. \\

\noindent
Sandu, C., Lenardic, A. and McGovern, P.J., 2011, The effects of deep water cycling on planetary thermal evolution, Journal of Geophysical Research, 116, B12404. \\

\noindent
Schubert, G., P. Cassen, and R. E. Young, 1979, Subsolidus convective cooling histories of terrestrial planets, Icarus, 38, 192–211. \\

\noindent
Schubert, G., D. Stevenson, and P. Cassen, 1980, Whole planet cooling and the radiogenic heat source contents of the Earth and Moon, J. Geophys. Res., 85, 2531–2538. \\

\noindent
Schubert, G., D. L. Turcotte, and P. Olson, 2001, Boundary layer theory, in Mantle Convection in the Earth and Planets, pp. 350–361, Cambridge Univ. Press, Cambridge, U. K. \\

\noindent
Solomatov, V.S., 1995, Scaling of temperature- and stress-dependent viscosity convection, Phys. Fluids, 7, 266-274. \\

\noindent
Turcotte, D.L. and Oxburgh, E.R. Finite amplitude convective cells and continental drift, J. Fluid Mech. 28 (1967) 29–42. \\

\noindent
Ulmer, P. and Trommsdorff, V., 1995, Serpentine stability to mantle depths and subduction-related magmatism, Science, 268(5212), 858–861. \\

\noindent
Weertman, J. and Weertman, J.R., 1975, High temperature creep of rock and mantle viscosity. Annual Review of the Earth and Planetary Sciences 3: 293–315. \\

\newpage

\end{document}

redpajama_set_name: RedPajamaArXiv


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Sheffield Hallam University Sports to manage all sports clubs with the MSL System
29th February 2017 - Sheffield Hallam University has chosen to implement the MSL System to support their 40+ sports clubs with a new website, membership management facilities, messaging capabilities, events, ecommerce, ticketing, community and feedback resources. The sports clubs will also utilise MSL's online elections platform for their annual committee officer elections.
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Published: 20 Feb 2017 15:19 , Last updated: 19 Nov 2019 15:28


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GREAT FOR KIDS: Are your days of frat parties and college soires long gone? This kid-friendly game is similar to tic-tac-toe, so it's easy to learn and play. Even toddlers can join in on the activities. Family game night just got more exciting.
FUN ON-THE-GO: With a sturdy carry and storage bag and simple assembly, this 4 in a row travel set is easy to transport and set-up. Include the combo pack at barbecues, camping trips, weddings, birthdays, pool parties, tailgates and backyard activities.
If you have any questions about this product by Rally & Roar, contact us by completing and submitting the form below. If you are looking for a specif part number, please include it with your message.


Cyrus Peikari, Seth Fogie, Ratter/29A, and Jonathan Read present a detailed two-part analysis of the Brador Trojan horse for the Windows Mobile operating system.
See Part 2 of of this article.
Recently we were the first to provide a detailed analysis and fix for WinCE4.Dust, the inaugural Pocket PC virus. We also gave the first detailed analysis of Mosquito, the inaugural Symbian Trojan horse. Now we're going to present a detailed analysis of Brador, the inaugural Trojan horse for the Windows Mobile operating system.
We weren't the first to discover Brador. We actually had a difficult time getting our hands on it. The author of WinCE4.Dust sent it to all antivirus (AV) companies, including ours (Airscanner). However, Brador was written by a different author, from Russia, who reportedly released it to only a select few "big" AV companies. As a smaller company that focuses exclusively on Windows Mobile antivirus software, we were left out in the cold.
The author, or perhaps his agent, was apparently selling copies of the client to interested parties for $150. With the client, anyone could take total control of a remote Pocket PC and steal passwords, empty bank accounts, or even penetrate "secure" corporate networks. (To put it into perspective, the Windows CE architecture is about as secure as a default Windows 95 installation was a decade ago.) However, no copy of the Trojan server itself could to be found. And we would never pay for a virus binary, as that would contribute to a market incentive for malware creation—a definite conflict of interest.
Fortunately, after mucking around in the underground for a while, we were able to obtain a copy of the Trojan, and we immediately started to reverse-engineer it. This article is our step-by-step investigation—not only of the Trojan, but also of the author, who until this article was not publicly known. We hope you will follow along to learn how to reverse-engineer for yourself. In this article, we use mostly free software tools, with the exception of IDA.


text:
Q: Unique lists in nested list in numba I would like to find the number of unique lists within a nested list in a nopython numba function, e.g:
from collections import Counter

def number_of_unique_lists_v1(a):
    uniques = Counter(tuple(item) for item in a)
    number = len(uniques.keys())
    return number

print(number_of_unique_lists_v1([[1,2,3],[1,2],[3,4],[1,2,3])
>>> 3

or
def number_of_unique_lists_v2(a):
    uniques = [list(x) for x in set(tuple(x) for x in a)]
    number = len(uniques)
    return number

print(number_of_unique_lists_v2([[1,2,3],[1,2],[3,4],[1,2,3])
>>> 3

Unfortunately, both ideas don't work with @nb.njit. How can I make it work?
Edit:
Using the approach of mpw2 I found that in principle the following code works:
from numba.typed import List
@nb.njit
def number_of_unique_lists_v3():
    a = [[1, 2, 3], [1, 2], [3, 4], [1, 2, 3]]
    s = List()
    for x in a:
        if not x in s:
            s.append(x)
    number = len(s)
    return number

print(number_of_unique_lists())
>>> 3

BUT this does not work for me since the list a  is created slightly differently in my function, similar as shown in a minimal example below.
from numba.typed import List
@nb.njit
def number_of_unique_lists():
    a = [[0] for _ in range(4)]
    a[0] = [1, 2, 3]
    a[1] = [1, 2]
    a[2] = [3, 4]
    a[3] = [1, 2, 3]
    s = List()
    for x in a:
        if not x in s:
            s.append(x)
    number = len(s)
    return number

Now I get an error which I don't understand...

A: Here is one working solution using numba.typed.List() objects
import numba as nb
from numba.typed import List

@nb.njit
def number_of_unique_lists(a):
    s = List()
    for x in a:
        if not x in s:
            s.append(x)
    number = len(s)
    return number

a = [[1,2,3],[1,2],[3,4],[1,2,3]]
typed_a = List()
for x in a:
    s = List()
    for y in x:
        s.append(y)
    typed_a.append(s)
print(number_of_unique_lists(typed_a))
>>> 3

redpajama_set_name: RedPajamaStackExchange


text:
Q: Android Set the text align to the middle of the toast I have a toast message which is pretty long. I would like to set the text in the middle and not to start align to the left.
Is this possible?

A: Toast is built on a TextView and the default gravity of it is left aligned. So, you need to create your own TextView like this for instance :
<TextView
android:layout_width="fill_parent"
android:layout_height="fill_parent"
android:gravity="center_vertical|center_horizontal"
android:text="all the text you want" />

And you assign the TextView to the Toast like this :
Toast t = new Toast(yourContext);
t.setView(yourNewTextView);

Source

A: Here:
Toast toast = Toast.makeText(this, "Message", Toast.LENGTH_SHORT);
toast.setGravity(Gravity.CENTER, 0, 0);
toast.show();


text:
package gov.nih.nci.caintegrator.domain.application;

/**
 * Indicates whether to search for up or down regulated genes in fold change query.
 */
public enum RegulationTypeEnum {

    /**
     * Up regulated.
     */
    UP("Up"),

    /**
     * Down regulated.
     */
    DOWN("Down"),

    /**
     * Up or down regulated.
     */
    UP_OR_DOWN("Up or Down"),

    /**
     * Up or down regulated.
     */
    UNCHANGED("Unchanged");

    private String value;

    private RegulationTypeEnum(String value) {
        this.value = value;
    }

    /**
     * @return the value
     */
    public String getValue() {
        return value;
    }

    /**
     * @param value the value to set
     */
    public void setValue(String value) {
        this.value = value;
    }
}


2018 Harley-Davidson® Softail® Fat Bob® The all-new Fat Bob features aggressive, unapologetic styling, mind-blowing performance and handling, premium finishes, and your choice of the powerful Milwaukee-Eight® 107 or 114 Big Twin Engine.
Harley-Davidson® Motorcycle Riding Boots & Casual Shoes Adventure starts with a single step. Walk away from the ordinary with motorcycle footwear crafted for true originals.
In the weeks since both companies reported first-quarter earnings near the end of April, Harley-Davidson's stock price has gained almost. in that statistic can have more to do with maintaining.
Some residents told the village board to take a hike if members OK a proposed Harley Davidson dealership in the heart of their community. building still there," said resident. The site is near a.
POWER. 2018 Harley-Davidson Fat Boy 114: The look of the Fat Boy® is more muscular than ever, thanks to all-new solid-disc wheels, and the 240mm rear tyre matched with a 160mm front.
2018 Iron 883 | Harley-Davidson UK. Aggressive throwback styling taken to a place altogether new. No need to shine this machine. Just get on and tear up the nearest street.
. Harley-Davidson® are H-D® dealerships in Cincinnati, Ohio & Florence, KY, featuring new and used vehicle types for sale, apparel, and accessories near.
View and Download Harley-Davidson Boom! Box owner's manual online. Boom! Box Car Navigation system pdf manual download.
EACH OF OUR LOCATIONS NOW HAS ITS OWN SITE!. So began the Hannum's Harley-Davidson® dynasty, which continues to bring the "Thrill of the Ride" to.
Quaid Harley-Davidson® located in Loma Linda, serves Southern California and offers. Working at a dealership in the past, I expected a good experience and.
Locate a Harley dealer near you. Find the Harley motorcycle that is right for you, learn to ride, schedule a test ride or shop for motorcycle parts & accessories.
Exterior Colour BLACK HILLS GOLD/BLACK QUARTZ • Odometer 21,500 • Comments 2017 Harley-Davidson® Road King® With this timeless combination of style and touring function you dont just ride through the landscape, youre the most majestic part of the scenery.
LAS VEGAS, Sept. 11, 2018 /PRNewswire/ — In show of support for the victims, families and first responders of 1 October, the Southern Nevada Harley-Davidson Dealers have announced the Vegas Strong.
Harley-Davidson® of Quantico is a H-D® motorcycle dealer in Dumfries, VA. We offer sales, parts, service, and rentals to Northeast Virginia, including Aquia.
Harley-Davidson® of Southampton is a premium Harley-Davidson® motorcycle dealership located in Southampton, MA. We offer motorcycles from the Harley®.
View and Download Harley-Davidson 2016 Boom! Box owner's manual online. 2016 Boom! Box Motorcycle Accessories pdf manual download.
Start A One-Machine Revolution. You have friends in the custom bike building business: the people at your local Harley-Davidson ® dealership. They eat, breathe and sleep Harley-Davidson.
Founded in 1912, A.D. Farrow is the nation's oldest Harley-Davidson dealer. It has three Columbus-area locations: off Interstate 71 at the interchange with Route 36/37 near Sunbury; on West Broad.
She says the couple's goal with the flagship store and other locations is to build Orlando's premier Harley-Davidson dealership. "I think that Orlando Harley-Davidson and the new historic dealership.
Latus Motors Harley-Davidson® is your motorcycle dealer in Clackamas. When you shop our dealership near Oregon City, you have the benefit of a staff who.
Phone: 973.898.7100 · Contact Us Map+Directions · Garden State Harley- Davidson® offers new and used motorcycles in Morris Plains and near.
"What a fantastic job you do," the president told his guests, who parked their five Harleys near the South Lawn. the blandishments of its Harley-Davidson Financial Services unit, which finances.
This is Harley-Davidson's fourth clutch related recall in the past. customers will have to visit their nearest dealership where a new secondary clutch actuator piston assembly will be installed at.
Harley-Davidson® Winnipeg in Winnipeg, MB, featuring new & used Harley-Davidson® motorcycles for sale, parts, service, and MotorClothes® near Kenora, Steinbach, Selkirk, and Fort Frances.
They might not be buying motorcycles at anywhere near the rate they once were. with someone they view as a more effective leader. Rumblings from Harley-Davidson's extensive dealer network indicate.
As if the economic recession alone is not enough of a threat, hundreds of Harley-Davidson dealers across the country are facing particularly challenging financial circumstances because they occupy.
https://www.biztimes.com/2019/industries/law/harley-seeking-6-3-million-from-new-berlin-janesville-dealerships/ Harley-Davidson's financing business is seeking nearly $6.3 million from the owner of.
Diving into the release a little further, "stronger dealers" apparently means "(enabling) best-performing and most entrepreneurial dealers to drive innovation and success for themselves and.
Pig Trail Harley-Davidson® is a motorcycle dealership with locations in Rogers & Eureka Springs, AR. We carry the latest Harley-Davidson® models. We also.
2018 Harley-Davidson® Softail® Fat Bob® 114 The all-new Fat Bob features aggressive, unapologetic styling, mind-blowing performance and handling, premium finishes, and your choice of the powerful Milwaukee-Eight® 107 or 114 Big Twin Engine.
They went on to add Harley-Davidson dealerships in Rochester, N.H., and Revere, Mass., outside Boston, and now operate four dealerships. "Shawn and I had been looking for a new, smaller store but also.
It will replace an existing Harley-Davidson store Cashman operates off the Strip, near Eastern and Sahara avenues. Cashman said he hopes tourists visiting the sign will cross the street to visit the.
They need good people so they can spend time in a home they are building near the ski slopes. art in a variety of media. The Harley dealership didn't come easily. There were long and complex.
Stop by Illinois H-D®, we're Chicago's premier Harley® dealer offering sales, service, parts, financing, and more!
Based on Harley's forecast for full-year bike shipments of between 241,000 to 246,000, that means it will be filling dealer. Harley-Davidson remains a financially sound company and it's still.
Exterior Colour White Hot Pearl • Odometer 26,150 • Comments 2013 Harley-Davidson® Road King® Classic. Take time to explore all of the 2013 Harley-Davidson® Road King® Classic FLHRC model features, including its detachable Harley® windshield.
Steel City Harley-Davidson® is a Harley-Davidson® dealer for new and used motorcycles as well as parts and services in Washington, Pennsylvania located.


SAN FRANCISCO — It is the urban driver's most agonizing everyday experience: the search for an empty parking place.
It is part sleuthing and part blood sport. Circling, narrowly missing a spot, outmaneuvering other motorists to finally ease into a space only to discover that it is off limits during working hours.
In this city, it is also a vexing traffic problem. Drivers cruising for parking spots generate 30 percent of all downtown congestion, city officials estimate.
Now San Francisco professes to have found a solution — a phone app for spot-seekers that displays information about areas with available spaces.
The system, introduced last month, relies on wireless sensors embedded in streets and city garages that can tell within seconds if a spot has opened up.


text:
K-Guard Is the Top Choice for Gutter Systems
At the high end of gutter protection systems is one that, unlike others, includes the gutters themselves, designed as a component of the system. Other products, whether hoods or micro-mesh filtering systems, are added to existing gutters, doing their best to protect channels for which they were not specifically engineered. No wonder problems abound after a heavy storm.
K-Guard gutter systems give consumers the real deal and the whole enchilada. 5-inch troughs are included, engineered to work in concert with their hoods, made of the same material in the same color. Hangers are also included and do not make contact with the roof, due consideration being given even to the height of the roof. It is easy to see that these features make K-Guard the top choice for gutter systems.
By the time new gutters, protectors, and fasteners are added to the cost of the toppers that constitute other protection systems, K-Guard gutter systems are competitively priced. Vastly superior to mix-and-match toppers that add a protection system to existing gutters, K-Guard gutter guards are more durable and more aesthetically pleasing. They essentially look like exterior crown molding.
The only gutter on the market to offer a rear drainage channel, the K-Guard gutter system gives water two ways to get in. Leaves and debris are kept out of the trough, providing a clog-free system for moving water away from the house. Because they are wider and able to accommodate larger downspouts, flushing is easier and drying faster.
Tucked under existing roof shingles, topper products eventually lift them, allowing water to get under the shingles and into the house. K-Guard gutter systems are attached directly to fascia board. Never touching the roof itself, these gutter protection systems leave roof warranties untouched as well. Cost effective, visually pleasing, and most importantly a top performer, K-Guard is the best choice a consumer can make.
Why You Should Have a Gutter Inspection
The parts of a home's gutter system that are difficult to access are the area's most likely to be damaged by corrosion and water damage. This is the principal reason for having an inspection on a yearly basis. While clogged downspouts may be easy to spot and clear, corroded fasteners are not, and fasteners that are not aligned properly can potentially cause a leak in the roof itself.
Even clogged downspouts need to be approached properly. Far from simply shoving a stick or tool of some kind up the spout to clear leaves and debris that are blocking it, which can damage the downspout, parts of the gutter may have to be removed in order to access the blocked area. Poking at blockages is a common way for homeowners to damage gutters.
If water is left in gutters, mold can develop within 48 hours. If that mold is simply allowed to remain around gutters, it can penetrate the house itself. In rare cases, it may even lead to black mold, which is a serious health hazard.
The metal flashing which attaches to the fascia at the edge of the roof is a problem spot. It secures the fascia and prevents leaks through the subfascia. Gutters are typically attached to it, either under it or against it. These attachment points need to be inspected for evidence of leaks or mold and, as mentioned, the fasteners need to be carefully checked.
Discolored siding, gutters, and eaves indicate leaks, and gutters that sag require immediate attention. A sagging gutter means either fasteners lost to corrosion or a rotting of the wood behind the fascia, probably due to a leak and the subsequent accumulation of water. Whatever the cause, gutters that sag result in water going where it is not wanted, up against the foundation of the house, which may cause dampness in the basement or an actual leak. A simple gutter inspection can save homeowners a lot of expense.


The Hcéres international team actively participates in international cooperation networks. It has forged close links with higher education stakeholders and developed substantial expertise in this field.
In association with the World Bank for the evaluation of several study programmes delivered by African centres of excellence.
With the French Development Agency (AFD) and the Commission des Titres d'ingénieur (Cti) for the organisation of a conference on quality assurance in Africa in October 2018, in addition to the production of a report on the actions carried out in this region.
Hcéres is also actively involved in monitoring international developments and contributes to European integration, while joining forces with countries all over the world in the framework of international funding projects.
developing quality assurance systems for higher education in Kazakhstan and Ukraine (EDUQAS).
to place Hcéres' recognised experience in quality assurance for higher education at the service of European integration and international developments.


text:
Q: Redirection loop when enabling Virtualhost HTTPS to HTTPS redirection I am using Apache sites to redirect HTTPS subdomain to other HTTPS subdomain but when I enable it I get a Redirection loop on the browser.
The initial situation is the following:
https://example1.domain.com and https://example2.domain.com shows the same content. The VirtualHost configuration is the following:
<VirtualHost *:443>
        ServerName example1.domain.com
        ServerAlias example2.domain.com
        DocumentRoot /srv/www/example1.domain.com/current/public
        SSLEngine on
        SSLCertificateFile    /srv/ssl/certs/server.crt
        SSLCertificateKeyFile /srv/ssl/certs/server.keyal
</VirtualHost>
The ideal situation would be example2.domain.com redirects to example1.domain.com and the application has only one access point. I am trying with the following VirtualHohst configuration:
<VirtualHost *:443>
        ServerAlias example2.domain.com
        Redirect permanent / https://example1.domain.com/
        SSLEngine on
        SSLCertificateFile    /srv/ssl/certs/server.crt
        SSLCertificateKeyFile /srv/ssl/certs/server.key
</VirtualHost>
<VirtualHost *:443>
        ServerName example1.domain.com
        DocumentRoot /srv/www/example1.domain.com/current/public
        SSLEngine on
        SSLCertificateFile    /srv/ssl/certs/server.crt
        SSLCertificateKeyFile /srv/ssl/certs/server.key
</VirtualHost>
But at this point I get a redirection loop on the browser.
Some ideas about the problem?

A: Change

ServerAlias example2.domain.com

to

ServerName example2.domain.com

It's not an alias there technically. I don't use Apache much anymore but it seems like because you told it it was an Alias, it keeps looking for a ServerName, hence the redirect loop.


text:
Tech Industries
Rural Enterprise
Cardiff Capital Region
South West Wales
Startup Wales
Appointments Wales
HR and People
Skills & Training
Showcasing the Best of Welsh Business
Supporting Employee Mental Health and Wellbeing in the Workplace During a Relationship Breakdown
A - Home Page B - Original Content HR & People
Ince , 19th October 2021
Susan J Williams,
Partner & Head of Family,
Ince (Cardiff)
One in four people will experience mental health issues in their lifetime. This can have a significant impact on a person's life, including their wellbeing and performance in the workplace.
In this article, Susan J Williams, Partner and Head of Family (Cardiff), explores the significant impact mental health can have on relationships, and its role as a cause and consequence of a relationship breakdown.
She also outlines how employers and HR professionals can support and promote good employee mental health and wellbeing – in particular, when they are experiencing difficulties in their relationship.
Everyone has both physical health and mental health. With physical ill health, it is normally visible and seen. However, mental health affects our emotional, psychological and social wellbeing, which is often not as visible. Therefore, it is not as easy to spot the signs of ill mental health as ill physical health.
Good mental health, as defined by the World Health Organisation is:
'a state of wellbeing in which every individual realises his or her own potential, can cope with the normal stresses of life, can work productively and fruitfully, and is able to make a contribution to her or his community'.
However, there are signs to look out for when a person is experiencing mental illness, these include:
Easily distracted
Being more worried and anxious
Finding it hard to make decisions
Having a low mood
Being disinterested in day to day activities
Having a feeling of being overwhelmed
Tearful and upset
Changes in mood
Poor eating and sleeping.
The above is a list of the more common signs, but it is not an exhaustive list, as mental ill health can affect people differently.
Looking after employee mental health during a relationship breakdown
Mental health can plays a crucial role in a relationship – when one partner is experiencing poor mental health, this can have a significant impact on the individual, their partner and their relationship – causing difficulties and sometimes a complete breakdown in the relationship. Likewise, the breakdown of a marriage or relationship can also result in one or both partners experiencing mental ill health – where the divorce process often intensifies the symptoms.
Relationship breakdowns and divorce are the second most stressful events in a person's life. Approximately a third of marriages end in divorce. In 2020, there were 107,599 divorces in England and Wales. Given on average that one in four people experience mental ill health in their lifetime, the statistics demonstrate the close correlation of mental ill health and relationship breakdowns.
There are so many changes and uncertainties around a relationship breakdown; from concerns about the children and what arrangements will need to be made, where everyone is going to live, how are the finances going to be divided between the couple, how long will it take to resolve – and what life will be like when it is all over. These are all large issues and can be overwhelming for many people.
Divorce is a huge life change, with high levels of stress that can have an enormous impact on someone's mental health. It is import that they are supported and have access to the help they need to get through this difficult period.
This is even more prevalent when domestic abuse is involved. Domestic abuse can happen to both women and men; and depression, anxiety and other mental health disorders are more significant where a person has experienced domestic abuse within a relationship.
Since the Covid-19 pandemic and numerous lockdowns of society, experts have seen an increase in people experiencing issues with their mental health. There is also growing evidence that during the pandemic there was also an increase in domestic violence.
As more and more employees continue to return to the workplace, it is important that employers and HR teams recognise how and why an employee is struggling with their mental health and the support and assistance they might need.
How can employers and HR teams support their employees with their mental health?
Employers have a duty of care to their employers to support their employees' health, wellbeing and safety. This includes mental health – and not just physical health. This involves both supporting employees experiencing poor mental health, and promoting good mental health practices more generally.
How can employers and HR teams promote good mental health practice in the workplace?
Ensure that employers and HR teams understand about mental health issues, and how to deal with these issues carefully and sensitively when they arise.
Stay alert to the early signs of stress, depression and anxiety. There should be procedures in place to ensure the proper response is given. Good communication is essential.
Properly signpost employees to their GP and/or organisations that could provide expert support such as MIND, domestic violence organisations such as Women's Aid and Mankind, as well as counsellors and solicitors.
Review the employee's role in the workplace to see whether there are areas that can be temporarily changed or modified to reduce stress and anxiety. This may assist in cases where stress in their home life is compounded with stress at work. Look at what adjustments can be made that would be the most helpful for the employee.
Consider whether you can offer flexible working or a staggered return to work where a member of staff is coming back to work after an extended period of absence. This is particularly relevant as employees return to work after the Covid-19 pandemic.
Inform and educate staff on mental health issues. Set up a mental health and wellbeing group to explore how to share information and good practices; introduce wellbeing initiatives at work, including training, workshops, use staff surveys; and consider starting mentoring or peer support schemes.
Create new mental health policies, which include strategies to remove the stigma around someone with mental ill health.
Explore the balance between work and life, and working from home and the office, which has become even more relevant following the Covid-19 pandemic.
Consider whether increased supervision or support is needed and how it can be provided within the workplace.
What are the benefits of a good approach to mental health issues in the workplace?
The role of mental health in the workplace is more important than ever, and employers and HR teams should prioritise their mental health workplace practices for the overall health of their organisation.
Having these practices in place will help employees when they are at their most vulnerable. Promoting positive mental health practices will help to reduce staff absences, increase the retention of staff, improve and maintain productivity, encourage employees to reach their full potential, and make your workplace a better place to be – where employees can feel valued and thrive.
Most people will manage their mental health with access the right support. World Mental Health Day took place on the 10 October 2021; raising awareness of mental health.
How can our Family team help?
Major events and changes in our lives, such as divorce, can significantly affect our mental health and wellbeing both at home and in the workplace. A greater understanding of mental health provides the opportunity for employers and HR teams to support their employees.
For more information and advice, get in touch with Susan J Williams, Partner and our Head of Family (Cardiff). Email [email protected] or call 07736969373 today, to see how we can support you and your employees.
The information above is not and should not be taken to be legal advice. You should not take action or omit to take action based on this information.
If you require any help on the issues raised above, please get in touch using the details above.
Welsh Local Authority Signs up to Support SMEs Tackle Cybercrime
Social Housing Pension Scheme 50% Contribution Rise Could Make Them Unaffordable
Ince has strong roots in Cardiff; as local solicitors Francis Ince and John Ingledew first set up practice here before founding the firm in 1870. We are proud of our heritage; which has enabled us to cultivate a seamless 'one-firm' approach across our global group.
We understand the ever-changing market in England and Wales, and how to support the growth of your business. Whether you are a business start-up or an established multinational corporation, through our Cardiff office you can access fully serviced commercial legal advice. Our Cardiff team also provides advice to individuals across the full-spectrum of personal law matters; from family law to residential property.
As a part of The Ince Group, an international legal and consultancy services provider with offices across Europe, the Middle East and Asia, we work seamlessly with other leading regional and international firms to offer you a wealth of legal services.
About Business News Wales
In creating Business News Wales, we aim to provide a voice for all Welsh businesses. With no political views or editorial agenda, our goal is to create the number one based source of business news in Wales, creating a level playing field for every business no matter of its size.
Report Sees Workforce Growth in Nearly a Third of Businesses Backed by Welsh Government Covid-19 Support
Development Bank of Wales, 1st February 2023
Cardiff University Appoints New Head of Commercialisation
Cardiff University, 1st February 2023
Theme Announced for the 2023 Swansea Conference
National News, 1st February 2023
Under a Fifth of SMEs Plan for Growth in 2023 According to ACCA
ACCA, 1st February 2023
Business Rates Revaluation: Key Considerations for Occupiers
Financial Services, 1st February 2023
Business News Wales from Business News Wales on Vimeo.
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text:
BioShock 2 Preview
Tags: #adam #big-daddy #big-sister #bioshock #bioshock-2 #little-sister #marin #multiplayer #preview #rapture
Companies: #2k-games
1 - BioShock 2 Preview 2 - BioShock 2 Impressions
Platform: PC, Xbox 360, PS3
Publisher: 2K Games
Release Date: February 9th 2010
BioShock was a great game and, while reactions to the supposed successor to System Shock have shifted somewhat since release from "this is awesome" to "this is consolified dross", we remain stalwart in our opinion. BioShock really was a fantastically ambitious and involving experience.
Still, it had problems – a lack of real replayability and multiplayer, plus one of the most underwhelming endings ever, to name a few. It also wasn't the type of game that would seem to lend itself all that well to further exploration and exploitation - an impression which left us with uneasy suspicion when we heard that a sequel was in the works.
BioShock introduced us to a brilliantly realised world and we loved every moment we spent in the fallen, underwater megalopolis of Rapture…but coming away from it we felt like perhaps we'd seen all that Andrew Ryan had to offer and that a follow-up would be more a rehash than anything truly worthwhile.
Even my little sister isn't this evil!
It's probably a good thing then that BioShock 2 (which has apparently dropped the 'Sea of Dreams' subtitle) is actually both a prequel and a sequel, with the singleplayer action set ten years after the original and the multiplayer couched in the civil war which destroyed Rapture. The decision to explore Rapture's past and the civil war which left it as the shattered shell we fell in love with will potentially allow the game to compensate for the familiar levels with a greater scale of conflict and a more intact world.
Rather than casting players as a simple Splicer or another interloper in Rapture's oceanic opulence though, BioShock 2 has made the unusual move of extrapolating the character from one of the most ill-judged areas of the climactic levels in the original game. You're a Big Daddy.
Well, not just any Big Daddy admittedly. You're the original Big Daddy. The first prototype who is endowed with enhanced movement and agility beyond what players were capable of in the first game, as well as free will. You've long been deactivated though and when you wake up in a long forgotten storage facility then you're not entirely sure what's going on – only that everybody is fighting and some powerful new factions have arisen in the chaos of this genetically modified war.
Predictably enough, you soon get involved in the politics of the war (because it'd be a short game if you just quietly departed or deactivated yourself once more). Unable to locate the original Little Sister that you were paired with, you sign up with the same tortured Dr. Tenenbaum who appeared in the first game and agree to help her try and save as much of Rapture as possible from the chaos which is enveloping it.
My big sister is probably even more evil though
There are new antagonists for you to go up against too, obviously. Both Andrew Ryan and Fontaine from the first game have been removed from the storyline, though there are some characters who reappear and guide you along. The new main baddies are the Big Sisters and a new character called Sophia Lamb - who is kind of an anti-Ryan.
The Big Sister is probably the one which BioShock 2 fans will know much about already – a sleeker, faster and more threatening variant of the Big Daddy who is fiercely protective of the Little Sisters and apparently has it in for you. The Big Sisters effectively take the role of the Big Daddies in the original game, with a finite amount of them littered through the levels for you to overcome. A much more serious threat than the relatively easy to defeat Daddies, a countdown sounds when Big Sis starts hunting for you and you'll have to quickly prepare yourself for the coming battle.
It's this idea we like most about the Big Sisters; the fact that they are actively hunting you and aren't purely reactionary enemies. One of the reasons the Big Daddies were so easy to kill in the first game was that you were always battling on your own terms and they'd only really respond if you got to close to a Little Sister. Having a more aggressive and agile foe who'll randomly show up and try to kill you is a brilliant way to bring tension to the game, even if it is very similar to the threat of stumbling across a Tank or Witch in Left 4 Dead 2.
BioShock 2 has no LAN or dedicated servers
2K Games has confirmed that BioShock 2 will have no dedicated server support, or LAN games.
January 28, 2010 | 12:01
BioShock 2 DRM detailed in full
2K has fully explained how DRM will work for the upcoming BioShock 2.
BioShock 2 available on Steam
Valve and 2K Games have announced that BioShock 2 is available to pre-purchase on Steam.