Since February 18, NASA has landed the perseverance probe on the ground of Mars . On board what the technicians call a demonstrator: a small drone. The mission that was entrusted to this small aircraft was to verify the feasibility of flight in the atmosphere of Mars. The planet has an atmosphere that has a density of 1% compared to that of the Earth. Only this data shows the technical difficulty of making the first Martian flight. Flight dynamics, as dimensioned on earth, are different from those present on the Red Planet. The next flights ( albeit short ) perhaps will see the drone rise to a higher altitude than already reached; it must be revealed how sustainable the flight is.

An interesting novelty in the field of wind turbines has recently appeared. It is a cylinder structured to" vibrate " when it is stressed by the wind. Compared to the well-known image of conventional wind turbines with the three blades of various sizes in relation to the capacity of electricity production, this type appears (currently ) as a pole about three meters high . The amount of energy it produces is currently small, but it has been shown to be able to produce it without environmental imperfections or subsonic frequency disturbances at the expense of animals. It is an excellent complement to solar panel technology. In many cases, in fact, the sunset coincides with the presence of breezes and winds given by the variation of temperatures between water and land, between hilly areas and plains etc. An aspect for the future moment could see this type of generator also on the surface of Mars. We consider the simple structure and possible modularity of the transport in assemblable sections on site. Recently the probes, which are already in action on the Martian soil, have transmitted to us the "voice" of the Martian wind.

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Earth’s modern atmosphere is highly oxygenated and is a remotely detectable signal of its surface biosphere. However, the lifespan of oxygen-based biosignatures in Earth’s atmosphere remains uncertain, particularly for the distant future. Here we use a combined biogeochemistry and climate model to examine the likely timescale of oxygen-rich atmospheric conditions on Earth. Using a stochastic approach, we find that the mean future lifespan of Earth’s atmosphere, with oxygen levels more than 1% of the present atmospheric level, is 1.08 ± 0.14 billion years (1σ). The model projects that a deoxygenation of the atmosphere, with atmospheric O2 dropping sharply to levels reminiscent of the Archaean Earth, will most probably be triggered before the inception of moist greenhouse conditions in Earth’s climate system and before the extensive loss of surface water from the atmosphere. We find that future deoxygenation is an inevitable consequence of increasing solar fluxes, whereas its precise timing is modulated by the exchange flux of reducing power between the mantle and the ocean–atmosphere–crust system. Our results suggest that the planetary carbonate–silicate cycle will tend to lead to terminally CO2-limited biospheres and rapid atmospheric deoxygenation, emphasizing the need for robust atmospheric biosignatures applicable to weakly oxygenated and anoxic exoplanet atmospheres and highlighting the potential importance of atmospheric organic haze during the terminal stages of planetary habitability. Main The field of exoplanet astronomy is on the verge of the first detailed characterization of the atmospheres of extrasolar planets, with heightened expectations for the potential detection of spectroscopic indicators of habitability, and possibly life, using the next generation of space- and ground-based telescopes1,2,3. However, a robust framework for remote life detection requires a detailed understanding of the factors that lead to the emergence and long-term maintenance of atmospheric biosignatures, including a full understanding of potential atmospheric compositions in the broader context of planetary biogeochemistry4. Although numerous potential atmospheric biosignatures have been proposed5, molecular oxygen (O2) and its photochemical by-product ozone (O3) remain at the forefront of approaches towards remote life detection owing to their strong absorption at visible and near-infrared wavelengths, the importance of biology in controlling their atmospheric abundances and the potential for homogeneity in abundance throughout the atmospheric column4,6. As a result, considerable effort has been directed towards understanding atmospheric oxygenation on habitable worlds and the factors that might lead to abiotic oxygen-rich atmospheres7,8,9. At present, Earth’s photosynthetic biosphere supports large gross fluxes of O2 to the ocean–atmosphere system—roughly 9 × 1015 mol O2 yr−1 (ref. 10)—with the result that the modern atmosphere is roughly 20% O2 by volume. However, the presence of oxygenic phototrophs on its own may not be enough to maintain a strongly oxygenated atmosphere. It is generally thought that the abundance of O2 in Earth’s atmosphere has been well below that of today for most of Earth’s history11, and that the modern atmospheric O2 abundance developed only after the emergence of land plants12,13, which have evolved to accelerate the geochemical cycles of bioessential elements (most importantly phosphorus) in Earth surface environments14,15. Thus, charting the history of planetary oxygenation after the evolution of oxygenic photosynthesis requires an understanding of how biospheric productivity (and the subsequent burial of reduced materials into sediments) changes in response to evolving environmental conditions. Previous work on the future lifespan of Earth’s biosphere has focused principally on the links between secular changes in solar luminosity, the stability of the carbonate–silicate geochemical cycle and the loss of surface water to space16,17,18,19,20. One robust result that emerges from this theoretical framework is a continuous decrease in the abundance of atmospheric CO2 through time, as steadily increasing solar luminosity inexorably drives down the abundance of atmospheric CO2 that is required to balance rates of crustal weathering with volcanic CO2 output16,17,21. However, several models suggest that, in spite of this thermal buffering mechanism, Earth will enter the moist greenhouse climate state at some point within approximately the next 2 billion years (Gyr)—a regime in which elevated atmospheric temperatures allow Earth’s stratosphere to become moist, leading to permanent water loss from Earth’s surface16,17,18,19,22,23. In addition, this drawdown of atmospheric CO2 may result in a fundamental shift to a photosynthetic biosphere that is CO2 limited—for instance, some models predict that terrestrial C3 plants will cease to be viable at Earth’s surface less than ~500 Myr into Earth’s future16. If true, this might place a long-term physical limit on the ability of photosynthetic biospheres to maintain high levels of atmospheric oxygen, giving rise to a fundamental trade-off between long-term stellar evolution, the geologic carbon cycle and the intrinsic timescale of atmospheric oxygenation. Here, we examine the future lifespan of Earth’s oxygenated atmosphere using a combined biogeochemistry and climate model (Fig. 1; Methods). Assessing the lifespan of Earth’s oxygenated atmosphere requires quantitative models that include a complete treatment of oxygen-related biogeochemical processes at the planetary surface over geologic time, as well as mechanistic linkages between surface environments and the planetary interior. Our model builds on previous similar Earth system models12 that track the coupled carbon, oxygen, phosphorus and sulfur cycles in the exogenic (that is, atmosphere, ocean and crust) system (Fig. 1). However, we extend this framework by incorporating a global biogeochemical methane (CH4) cycle, including a range of key biological metabolisms, parameterized atmospheric photochemistry within the O2–O3–CH4 system24,25 and the radiative impact of CH4 on the global energy balance26. Our model also explicitly evaluates redox exchange between the crust and mantle, allowing a comprehensive evaluation of the planetary processes controlling atmospheric O2 levels over geologic time. The model is designed to capture the major components of Earth system biogeochemistry and climate, but is abstracted enough to allow for large model ensembles that can be run for billions of years of model time. Fig. 1: Schematic model structure. figure1 Boxes denote reservoirs, whereas arrows denote flux terms. The model tracks the major reservoirs and transfer fluxes within the surface carbon, sulfur, oxygen and phosphorus cycles, along with a comprehensive treatment of ocean biogeochemistry and long-term transfers between the crust–ocean–atmosphere system and the mantle. Atm, atmosphere; DIC, dissolved inorganic carbon; ALK, alkalinity; DOA, degree of anoxia. Full size image We employed a stochastic approach in which we drew randomly from a wide range of potential values for parameters controlling the major geophysical boundary conditions of the model, including variability (cycle and amplitude) in outgassing rates and erosional forcing (Methods and Extended Data Figs. 1–3), and initialized the model at 600 Myr ago (Ma). We then repeatedly ran the model forward in time until the present day (n = ~400,000), and subsampled model runs (n = 4,787) that roughly reproduced modern atmospheric composition (using atmospheric mixing ratios of O2 and CO2 of 20% T0 (273 K). For Tice < Ts < T0, the albedo is interpolated with a quadratic interpolation method62. RFCH4 represents the radiative forcing by methane, which is quantified on the basis of ref. 26. Recent 1D modelling results suggest that relatively small increases in solar luminosity could conceivably trigger a runaway greenhouse on Earth63,64. However, 3D climate models indicate that Earth’s climate is likely to be more stable than this as a consequence of the expansion of unsaturated regions in the upper atmosphere attendant to changes in Hadley circulation that occur at higher solar fluxes23,65. Given the quantitative consistency between the above 0D energy balance model and recent 3D climate models35 (Supplementary Fig. 1), we consider our utilization of a zero-dimensional energy balance model a defensible approximation of planetary climate for implementation on 106−109 yr timescales. Nevertheless, it is important to point out that future projections of Earth system behaviour will probably be modulated by uncertain cloud feedbacks and continental configurations. As a result, in our Monte Carlo analysis we explored uncertainties in OLR and TOA (Extended Data Fig. 3). Stochastic analysis The computational efficiency of the model enabled us to examine the future lifespan of the oxygenated atmosphere via a stochastic analysis, in which we randomly sampled from a prior distribution for poorly constrained parameters and quantified whole-model uncertainty (Extended Data Fig. 3). We drew poorly constrained initial values for crustal C and S reservoir sizes at 600 Ma over a wide range of values. We also varied the reference values of fluxes between the exogenic system and the mantle (subduction and mantle degassing) to capture uncertainties in model parameterization. After running the model forward in time until the present, we only sampled model runs that allowed for acceptable atmospheric composition (20%

Space, The Last Frontier. A curiosity related to this new generation of settlers. Economic treatment. An astronaut earns enough, but not as much as one might imagine. Nasa civilian astronauts are classified as GS-12 and GS-13 civil servants, depending on their skills and seniority. According to the salaries of 2020, for them we speak of a figure between 66, 167 and 161, 141 gross dollars per year. In euros, they are between 55.000 and 134.000 euros a year gross, which net become between 42.000 and 91.000 approximately. Figures perhaps lower than the expectations of our fantasies? It is the call of the frontier; it is the call of knowledge.

Hi  Shall we meet on meet? So we can talk about our project, ideas or only chatting!!!🤣  Did I create a code ?  See you

I recently discovered that at the University of Rome, the Sioi has a master in space trade legislation and space policies. I think it's a good launch point for our boys who want to get into a new future. In view of the fact that we will need to relate to other countries, to understand how we intend to legislate space is not to be underestimated. How many of you have sons of a univeritarian age? Would it be possible to start training in this direction?m Thank you

That guy in the picture is me! 😏 I apologize to my followers if I don't often publish stories, I've a busy life. In these 3 years I think no one would have expected Asgardia to grow so much to reach the whole world! But I, although I am a skeptic, I was one of the few to believe in this huge project! From the very beginning! After a long time of absence, here I'm again Asgardia! ✌🏽

[...] Uno stile o un disagio? Può un nuovo ordine dipingere progresso sociale collettivo è possa soddisfare le nuove e vecchie generazioni analogiche, digitali e Quantistiche esistenti integrate e operative ? Meglio partecipe che ignaro [...] del nuovo ordine, se continua così, progredendo verso i beni e i servizi, senza guardare la vera maschera che porta avanti la giustizia e l’ordine collettivo creatosi, si potrà o si deve, restare e possedere Capacità con possibilità di sussistere e di operare in base a principi di assoluta autonomia ?