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Gnaeus Papirius Carbo (d.81 BC)
Gnaeus Papirius Carbo (d.81 BC) was the main leader of the Marian faction during Sulla's Second Civil War, and was killed after fleeing into exile in Africa as his cause began to collapse.
Carbo was the son of another Gn. Papirius Carbo, one of the consuls for 113 BC. He committed suicide after he was defeated by the Cimbri at the battle of Noreia (112 BC).
The younger Carbo served as tribune of the plebs in 92 BC. During his time in this post a meeting of the people got out of control, and he was blamed. A law was passed making the person who proposed a law responsible for any disorder caused by its discussion. He also put forward a law on the use of the secret ballot in some forms of voting.
Carbo joined the anti-Sullan forces during Sulla's First Civil War, and took part in the siege of Rome of 87 BC, where he served alongside the consul Cinna and was posted 'opposite' the city walls, presumably besieging the walls facing away from the Tiber (Sertorius was posted above Rome on the Tiber and Marius between Rome and the sea). He then accompanied the Marian army as it moved away from Rome, and camped about 11 miles from the city, after cutting off supplies. Sulla's supporters made the mistake of leaving the city to face Cinna and Marius, and lost control of Rome. Cinna and Marius were invited in, the pro-Sullan Consul G. Octavius was killed, and Marius began a reign of terror that was ended by his death early in 86 BC.
The leadership of the Marian faction then fell to Cinna, who served as consul in 86, 85 and 84 BC. Carbo was his co-consul in 85 and 84 BC. When it became clear that Sulla was winning the war against Mithridates VI of Pontus, and would soon be free to return to Italy, Cinna and Carbo began to raise fresh armies, while also selecting themselves as the consuls for 83 BC. Cinna decided to take the battle to Sulla in the Balkans, but this badly backfired. The second detachment to cross the Adriatic was turned back by a storm and deserted once they were safely back in Italy. The rest of the army then refused to risk the crossing. Cinna attempted to put down the mutiny, but mishandled the situation and was murdered. Carbo was thus left in sole command, and refused to hold an election for a replacement for Cinna. However he also decided not to hold the consulship for 83 BC, which instead went to Gaius Norbanus and Lucius Cornelius Scipio Asiaticus. Carbo became the proconsul for Gaul for 83 BC.
Sulla invaded Italy in 83 BC. Carbo's role at the start of the war (Sulla's Second Civil War) isn't entirely clear. Plutarch reports that he commanded one of a series of armies sent to deal with the young Pompey, who was raising an army for Sulla in Picenum, but the details of this campaign appear to duplicate events elsewhere. In the second battle Scipio lost the loyaly of his army, which switched sides, and in the third Carbo is said to have been defeated in battle on the River Aesis. However Scipio lost the loyalty of his army in a better documented encounter against Sulla at Teanum, while one of Carbo's lieutenants was defeated on the Aesis in the first battle of 82 BC. These are probably the genuine incidents, rather than the versions of 83 BC.
As Sulla advanced towards Rome in 83 BC the two consuls both suffered defeats. Norbanus was defeated in battle at Casilinium or Mount Tifata, on the Volturnus River. Scipio agreed to peace talks at Teanum, a few miles to the north, where Sulla was able to convince his entire army to change sides. After this disaster Carbo is reported to have said that 'In making war upon the fox and the lion in Sulla, he was more annoyed by the fox'.
Carbo, who had probably accompanied one of these armies, rushed back to Rome, where he secured control of the city, and had Sulla's supporters declared public enemies. At about this point the Temple of Jupiter on the Capital burnt down, and some blamed Carbo for the disaster, but it wasn't clear if this was the case at the time. The campaign of 83 BC then began to wind down.
Carbo decided to serve as one of the consuls for 82 BC, alongside Marius the Younger, son of Gaius Marius, and despite his young age an powerful recruiting tool. Marius was given the task of facing Sulla to the south of Rome, while Carbo went north to deal with Metellus Pius and the young Pompey. We now come to the more likely battle of the Aesis, where Carbo's lieutenant Carinnas was defeated by Metellus at the river on the northern border of Picenum. Carbo then arrived and restored the situation, and forced Metellus to retreat north. He then besieged him at an unnamed location somewhere to the north of Ariminum (Rimini).
Carbo was soon forced to abandon the siege after bad news came from the south. Marius had been defeated at Sacriportus, and was now besieged in Praeneste. Carbo retreated back to Ariminum, with Pompey harassing him. He then continued to head back towards Rome, but he was beaten to the city by Sulla. Carbo stopped at Clusium, on the River Glanis, about eighty miles to the north of Rome.
Carbo now had three armies on different approaches to Rome. He was at Clusium, on the Via Cassia. To the west was a second force at Saturnia, on the Via Flaminia. To the east Carinnas was close to Spoletium, on the Via Clodia. He had also received some reinforcements - Celtiberian cavalry sent by the governors of Spain.
Sulla moved north from Rome. He defeated part of the Celtiberian cavalry on the Glanis River, and another 270 deserted to him. In response Carbo massacred the remaining cavalrymen, either as punishment or because he feared they would do the same. To the west Sulla's men defeated the detachment at Saturnia. This was followed by a day long battle between Sulla and Carbo (first battle of Clusium), but this ended inconclusively. Carbo probably retained control of the battlefield, but Sulla remained nearby.
To the east Pompey defeated Carinnas on the plains of Spoletium, and besieged him in the town. Carbo sent a force to try and lift the siege, but they were ambushed by Sulla and defeated. Carinnas still managed to escape under the cover of a storm.
Carbo's next move was to send Marcius with eight legions to try and raise the siege of Praeneste. This time Pompey ambushed the relief force, and Marcius escaped with only seven cohorts.
The Marians were now given the boost by the arrival of a large Italian army, of 70,000 Samnites and Lucanians, which threatened to lift the siege of Praeneste. Sulla was forced to dash south to prevent the Samnites from rescuing Marius, leaving Carbo free to dash north in an attempt to defeat Metellus Pius, who was still in Cisalpine Gaul.
This attack went disastrously wrong (Battle of Faventia). Carbo attempted a night attack, but his troops got caught up in vineyards, and Metellus was able to counterattack. Carbo lost most of his army - 10,000 dead and deserters - and he returned to Ariminum with only 1,000 men under arms. His ally Norbanus, who had also been involved in the disaster, decided that the war was lost and fled into exile in the east.
Carbo returned to his army north of Rome. He made one last attempt to raise the siege of Praeneste, sending Brutus Damasippus with two legions to try and break through Sulla's blocking force, but this effort failed. Soon afterwards news arrived that one of Carbo's armies had been defeated near Placentia, and the Gauls of Cisalpine Gaul had changed sides. Although Carbo still had at least 40,000 troops under his own command, this new broke his nerve, and he fled into exile in Africa.
Carbo didn't survive for long in exile. After Sulla had completed his victory in Italy, he sent Pompey to attack the Marian governor of Sicily. This was bad timing for Carbo, who had only just arrived in Sicily himself. He narrowly escaped from Pompey's men, and retreated to Cossyra (Pantellaria), but soon afterwards he fell into Pompey's hands. Pompey's reputation rather suffered after he interviewed Carbo before having him executed - other prisoners had been executed without being humiliated in the same way. Carbo's head was then sent to Sulla.
Gnaeus Papirius Carbo (consul 113 BC)
Gnaeus Papirius Carbo, son of Gaius Papirius Carbo, was Roman consul in 113 BC, together with Gaius Caecilius Metellus Caprarius.
He was according to Cicero (ad Fam. ix. 21) the father of Gnaeus Papirius Carbo, who was thrice consul, whereas this latter is called by Velleius Paterculus (II 26) a brother of Gaius Papirius Carbo Arvina. This difficulty may be solved by supposing that the word frater in Velleius is equivalent to frater patruelis or cousin. (Perizon., Animadv. Hist. p.㻠.) In his consulship the Cimbri advanced from Gaul into Italy and Illyricum, and Carbo, who was sent against them, was put to flight with his whole army. He was afterwards accused by Marcus Antonius Orator, we know not for what reason, and put an end to his own life by taking a solution of vitriol (atramentum sutorium, Cic., ad Fam. IX 21 Liv., Epit. 63.).
|Preceded by |
Manius Acilius Balbus and Gaius Porcius Cato
| Consul of the Roman Republic |
with Gaius Caecilius Metellus Caprarius
|Succeeded by |
Lucius Calpurnius Piso Caesoninus and Marcus Livius Drusus
Information as of: 13.07.2020 02:22:55 CEST
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Carbon dioxide concentrations have shown several cycles of variation from about 180 parts per million during the deep glaciations of the Holocene and Pleistocene to 280 parts per million during the interglacial periods. Following the start of the Industrial Revolution, atmospheric CO
2 concentration increased to over 400 parts per million and continues to increase, causing the phenomenon of global warming.  As of April 2019 [update] , the average monthly level of CO
2 in Earth's atmosphere exceeded 413 parts per million.  The daily average concentration of atmospheric CO
2 at Mauna Loa Observatory first exceeded 400 ppm on 10 May 2013   although this concentration had already been reached in the Arctic in June 2012.  Each part per million by volume of CO
2 in the atmosphere represents approximately 2.13 gigatonnes of carbon, or 7.82 gigatonnes of CO
2 .  As of 2018, CO
2 constitutes about 0.041% by volume of the atmosphere, (equal to 410 ppm)      which corresponds to approximately 3210 gigatonnes of CO
2 , containing approximately 875 gigatonnes of carbon. The global mean CO
2 concentration is currently rising at a rate of approximately 2 ppm/year and accelerating.   The current growth rate at Mauna Loa is 2.50 ± 0.26 ppm/year (mean ± 2 std dev).  As seen in the graph to the right, there is an annual fluctuation – the level drops by about 6 or 7 ppm (about 50 Gt) from May to September during the Northern Hemisphere's growing season, and then goes up by about 8 or 9 ppm. The Northern Hemisphere dominates the annual cycle of CO
2 concentration because it has much greater land area and plant biomass than the Southern Hemisphere. Concentrations reach a peak in May as the Northern Hemisphere spring greenup begins, and decline to a minimum in October, near the end of the growing season.  
Since global warming is attributed to increasing atmospheric concentrations of greenhouse gases such as CO
2 and methane, scientists closely monitor atmospheric CO
2 concentrations and their impact on the present-day biosphere. The National Geographic wrote that the concentration of carbon dioxide in the atmosphere is this high "for the first time in 55 years of measurement—and probably more than 3 million years of Earth history."  The current concentration may be the highest in the last 20 million years. 
Carbon dioxide concentrations have varied widely over the Earth's 4.54 billion year history. It is believed to have been present in Earth's first atmosphere, shortly after Earth's formation. The second atmosphere, consisting largely of nitrogen and CO
2 was produced by outgassing from volcanism, supplemented by gases produced during the late heavy bombardment of Earth by huge asteroids.  A major part of carbon dioxide emissions were soon dissolved in water and incorporated in carbonate sediments.
The production of free oxygen by cyanobacterial photosynthesis eventually led to the oxygen catastrophe that ended Earth's second atmosphere and brought about the Earth's third atmosphere (the modern atmosphere) 2.4 billion years before the present. Carbon dioxide concentrations dropped from 4,000 parts per million during the Cambrian period about 500 million years ago to as low as 180 parts per million during the Quaternary glaciation of the last two million years. 
Drivers of ancient-Earth CO2 concentration Edit
On long timescales, atmospheric CO
2 concentration is determined by the balance among geochemical processes including organic carbon burial in sediments, silicate rock weathering, and volcanic degassing. The net effect of slight imbalances in the carbon cycle over tens to hundreds of millions of years has been to reduce atmospheric CO
2 . On a timescale of billions of years, such downward trend appears bound to continue indefinitely as occasional massive historical releases of buried carbon due to volcanism will become less frequent (as earth mantle cooling and progressive exhaustion of internal radioactive heat proceed further). The rates of these processes are extremely slow hence they are of no relevance to the atmospheric CO
2 concentration over the next hundreds or thousands of years.
In billion-year timescales, it is predicted that plant, and therefore animal, life on land will die off altogether, since by that time most of the remaining carbon in the atmosphere will be sequestered underground, and natural releases of CO
2 by radioactivity-driven tectonic activity will have continued to slow down.  [ better source needed ] The loss of plant life would also result in the eventual loss of oxygen. Some microbes are capable of photosynthesis at concentrations of CO
2 of a few parts per million and so the last life forms would probably disappear finally due to the rising temperatures and loss of the atmosphere when the sun becomes a red giant some four billion years from now. 
Measuring ancient-Earth CO2 concentration Edit
The most direct method for measuring atmospheric carbon dioxide concentrations for periods before instrumental sampling is to measure bubbles of air (fluid or gas inclusions) trapped in the Antarctic or Greenland ice sheets. The most widely accepted of such studies come from a variety of Antarctic cores and indicate that atmospheric CO
2 concentrations were about 260–280 ppmv immediately before industrial emissions began and did not vary much from this level during the preceding 10,000 years.  The longest ice core record comes from East Antarctica, where ice has been sampled to an age of 800,000 years.  During this time, the atmospheric carbon dioxide concentration has varied between 180 and 210 ppm during ice ages, increasing to 280–300 ppm during warmer interglacials.   The beginning of human agriculture during the current Holocene epoch may have been strongly connected to the atmospheric CO
2 increase after the last ice age ended, a fertilization effect raising plant biomass growth and reducing stomatal conductance requirements for CO
2 intake, consequently reducing transpiration water losses and increasing water usage efficiency. 
Various proxy measurements have been used to attempt to determine atmospheric carbon dioxide concentrations millions of years in the past. These include boron and carbon isotope ratios in certain types of marine sediments, and the number of stomata observed on fossil plant leaves. 
Phytane is a type of diterpenoid alkane. It is a breakdown product of chlorophyll and is now used to estimate ancient CO
2 levels.  Phytane gives both a continuous record of CO
2 concentrations but it also can overlap a break in the CO
2 record of over 500 million years. 
There is evidence for high CO
2 concentrations between 200 and 150 million years ago of over 3,000 ppm, and between 600 and 400 million years ago of over 6,000 ppm.  In more recent times, atmospheric CO
2 concentration continued to fall after about 60 million years ago. About 34 million years ago, the time of the Eocene–Oligocene extinction event and when the Antarctic ice sheet started to take its current form, CO
2 was about 760 ppm,  and there is geochemical evidence that concentrations were less than 300 ppm by about 20 million years ago. Decreasing CO
2 concentration, with a tipping point of 600 ppm, was the primary agent forcing Antarctic glaciation.  Low CO
2 concentrations may have been the stimulus that favored the evolution of C4 plants, which increased greatly in abundance between 7 and 5 million years ago.  Based on an analysis of fossil leaves, Wagner et al.  argued that atmospheric CO
2 concentrations during the last 7,000–10,000 year period were significantly higher than 300 ppm and contained substantial variations that may be correlated to climate variations. Others have disputed such claims, suggesting they are more likely to reflect calibration problems than actual changes in CO
2 .  Relevant to this dispute is the observation that Greenland ice cores often report higher and more variable CO
2 values than similar measurements in Antarctica. However, the groups responsible for such measurements (e.g. H.J. Smith et al.  ) believe the variations in Greenland cores result from in situ decomposition of calcium carbonate dust found in the ice. When dust concentrations in Greenland cores are low, as they nearly always are in Antarctic cores, the researchers report good agreement between measurements of Antarctic and Greenland CO
Earth's natural greenhouse effect makes life as we know it possible and carbon dioxide plays a significant role in providing for the relatively high temperature that the planet enjoys. The greenhouse effect is a process by which thermal radiation from a planetary atmosphere warms the planet's surface beyond the temperature it would have in the absence of its atmosphere.    Without the greenhouse effect, the Earth's temperature would be about −18 °C (−0.4 °F)   compared to Earth's actual surface temperature of approximately 14 °C (57.2 °F). 
Carbon dioxide is believed to have played an important effect in regulating Earth's temperature throughout its 4.7 billion year history. Early in the Earth's life, scientists have found evidence of liquid water indicating a warm world even though the Sun's output is believed to have only been 70% of what it is today. It has been suggested by scientists that higher carbon dioxide concentrations in the early Earth's atmosphere might help explain this faint young sun paradox. When Earth first formed, Earth's atmosphere may have contained more greenhouse gases and CO
2 concentrations may have been higher, with estimated partial pressure as large as 1,000 kPa (10 bar), because there was no bacterial photosynthesis to reduce the gas to carbon compounds and oxygen. Methane, a very active greenhouse gas which reacts with oxygen to produce CO
2 and water vapor, may have been more prevalent as well, with a mixing ratio of 10 −4 (100 parts per million by volume).  
Though water is responsible for most (about 36-70%) of the total greenhouse effect, the role of water vapor as a greenhouse gas depends on temperature. On Earth, carbon dioxide is the most relevant, direct anthropologically influenced greenhouse gas. Carbon dioxide is often mentioned in the context of its increased influence as a greenhouse gas since the pre-industrial (1750) era. In the IPCC Fifth Assessment Report the increase in CO2 was estimated to be responsible for 1.82 W m −2 of the 2.63 W m −2 change in radiative forcing on Earth (about 70%). 
The concept of atmospheric CO2 increasing ground temperature was first published by Svante Arrhenius in 1896.  The increased radiative forcing due to increased CO2 in the Earth's atmosphere is based on the physical properties of CO2 and the non-saturated absorption windows where CO2 absorbs outgoing long-wave energy. The increased forcing drives further changes in Earth's energy balance and, over the longer term, in Earth's climate. 
Atmospheric carbon dioxide plays an integral role in the Earth's carbon cycle whereby CO
2 is removed from the atmosphere by some natural processes such as photosynthesis and deposition of carbonates, to form limestones for example, and added back to the atmosphere by other natural processes such as respiration and the acid dissolution of carbonate deposits. There are two broad carbon cycles on Earth: the fast carbon cycle and the slow carbon cycle. The fast carbon cycle refers to movements of carbon between the environment and living things in the biosphere whereas the slow carbon cycle involves the movement of carbon between the atmosphere, oceans, soil, rocks, and volcanism. Both cycles are intrinsically interconnected and atmospheric CO
2 facilitates the linkage.
Natural sources of atmospheric CO
2 include volcanic outgassing, the combustion of organic matter, wildfires and the respiration processes of living aerobic organisms. Man-made sources of CO
2 include the burning of fossil fuels for heating, power generation and transport, as well as some industrial processes such as cement making. It is also produced by various microorganisms from fermentation and cellular respiration. Plants, algae and cyanobacteria convert carbon dioxide to carbohydrates by a process called photosynthesis. They gain the energy needed for this reaction from absorption of sunlight by chlorophyll and other pigments. Oxygen, produced as a by-product of photosynthesis, is released into the atmosphere and subsequently used for respiration by heterotrophic organisms and other plants, forming a cycle with carbon.
Most sources of CO
2 emissions are natural, and are balanced to various degrees by similar CO
2 sinks. For example, the decay of organic material in forests, grasslands, and other land vegetation - including forest fires - results in the release of about 436 gigatonnes of CO
2 (containing 119 gigatonnes carbon) every year, while CO
2 uptake by new growth on land counteracts these releases, absorbing 451 Gt (123 Gt C).  Although much CO
2 in the early atmosphere of the young Earth was produced by volcanic activity, modern volcanic activity releases only 130 to 230 megatonnes of CO
2 each year.  Natural sources are more or less balanced by natural sinks, in the form of chemical and biological processes which remove CO
2 from the atmosphere. By contrast, as of year 2019 the extraction and burning of geologic fossil carbon by humans releases over 30 gigatonnes of CO
2 (9 billion tonnes carbon) each year.  This larger disruption to the natural balance is responsible for recent growth in the atmospheric CO
2 concentration.  
Overall, there is a large natural flux of atmospheric CO
2 into and out of the biosphere, both on land and in the oceans.  In the pre-industrial era, each of these fluxes were in balance to such a degree that little net CO
2 flowed between the land and ocean reservoirs of carbon, and little change resulted in the atmospheric concentration. From the human pre-industrial era to 1940, the terrestrial biosphere represented a net source of atmospheric CO
2 (driven largely by land-use changes), but subsequently switched to a net sink with growing fossil carbon emissions.  In 2012, about 57% of human-emitted CO
2 , mostly from the burning of fossil carbon, was taken up by land and ocean sinks.  
The ratio of the increase in atmospheric CO
2 to emitted CO
2 is known as the airborne fraction (Keeling et al., 1995). This ratio varies in the short-term and is typically about 45% over longer (5-year) periods.  Estimated carbon in global terrestrial vegetation increased from approximately 740 gigatonnes in 1910 to 780 gigatonnes in 1990.  By 2009, oceanic neutralization had decreased the pH of seawater by 0.11 due to uptake of emitted CO
2 . 
Atmospheric CO2 and photosynthesis Edit
Carbon dioxide in the Earth's atmosphere is essential to life and to most of the planetary biosphere. Over the course of Earth's geologic history CO
2 concentrations have played a role in biological evolution. The first photosynthetic organisms probably evolved early in the evolutionary history of life and most likely used reducing agents such as hydrogen or hydrogen sulfide as sources of electrons, rather than water.  Cyanobacteria appeared later, and the excess oxygen they produced contributed to the oxygen catastrophe,  which rendered the evolution of complex life possible. In recent geologic times, low CO
2 concentrations below 600 parts per million might have been the stimulus that favored the evolution of C4 plants which increased greatly in abundance between 7 and 5 million years ago over plants that use the less efficient C3 metabolic pathway.  At current atmospheric pressures photosynthesis shuts down when atmospheric CO
2 concentrations fall below 150 ppm and 200 ppm although some microbes can extract carbon from the air at much lower concentrations.   Today, the average rate of energy capture by photosynthesis globally is approximately 130 terawatts,    which is about six times larger than the current power consumption of human civilization.  Photosynthetic organisms also convert around 100–115 billion metric tonnes of carbon into biomass per year.  
Photosynthetic organisms are photoautotrophs, which means that they are able to synthesize food directly from CO
2 and water using energy from light. However, not all organisms that use light as a source of energy carry out photosynthesis, since photoheterotrophs use organic compounds, rather than CO
2 , as a source of carbon.  In plants, algae and cyanobacteria, photosynthesis releases oxygen. This is called oxygenic photosynthesis. Although there are some differences between oxygenic photosynthesis in plants, algae, and cyanobacteria, the overall process is quite similar in these organisms. However, there are some types of bacteria that carry out anoxygenic photosynthesis, which consumes CO
2 but does not release oxygen.
Carbon dioxide is converted into sugars in a process called carbon fixation. Carbon fixation is an endothermic redox reaction, so photosynthesis needs to supply both the source of energy to drive this process and the electrons needed to convert CO
2 into a carbohydrate. This addition of the electrons is a reduction reaction. In general outline and in effect, photosynthesis is the opposite of cellular respiration, in which glucose and other compounds are oxidized to produce CO
2 and water, and to release exothermic chemical energy to drive the organism's metabolism. However, the two processes take place through a different sequence of chemical reactions and in different cellular compartments.
Most organisms that utilize photosynthesis to produce oxygen use visible light to do so, although at least three use shortwave infrared or, more specifically, far-red radiation. 
Effects of increased CO2 on plants and crops Edit
A 1993 review of scientific greenhouse studies found that a doubling of CO
2 concentration would stimulate the growth of 156 different plant species by an average of 37%. Response varied significantly by species, with some showing much greater gains and a few showing a loss. For example, a 1979 greenhouse study found that with doubled CO
2 concentration the dry weight of 40-day-old cotton plants doubled, but the dry weight of 30-day-old maize plants increased by only 20%.  
In addition to greenhouse studies, field and satellite measurements attempt to understand the effect of increased CO
2 in more natural environments. In free-air carbon dioxide enrichment (FACE) experiments plants are grown in field plots and the CO
2 concentration of the surrounding air is artificially elevated. These experiments generally use lower CO
2 levels than the greenhouse studies. They show lower gains in growth than greenhouse studies, with the gains depending heavily on the species under study. A 2005 review of 12 experiments at 475–600 ppm showed an average gain of 17% in crop yield, with legumes typically showing a greater response than other species and C4 plants generally showing less. The review also stated that the experiments have their own limitations. The studied CO
2 levels were lower, and most of the experiments were carried out in temperate regions.  Satellite measurements found increasing leaf area index for 25% to 50% of Earth's vegetated area over the past 35 years (i.e., a greening of the planet), providing evidence for a positive CO2 fertilization effect.  
A 2017 Politico article states that increased CO
2 levels may have a negative impact on the nutritional quality of various human food crops, by increasing the levels of carbohydrates, such as glucose, while decreasing the levels of important nutrients such as protein, iron, and zinc. Crops experiencing a decrease in protein include rice, wheat, barley and potatoes.  [ scientific citation needed ]
Atmospheric CO2 and the oceanic carbon cycle Edit
The Earth's oceans contain a large amount of CO
2 in the form of bicarbonate and carbonate ions—much more than the amount in the atmosphere. The bicarbonate is produced in reactions between rock, water, and carbon dioxide. One example is the dissolution of calcium carbonate:
Reactions like this tend to buffer changes in atmospheric CO
2 . Since the right side of the reaction produces an acidic compound, adding CO
2 on the left side decreases the pH of seawater, a process which has been termed ocean acidification (pH of the ocean becomes more acidic although the pH value remains in the alkaline range). Reactions between CO
2 and non-carbonate rocks also add bicarbonate to the seas. This can later undergo the reverse of the above reaction to form carbonate rocks, releasing half of the bicarbonate as CO
2 . Over hundreds of millions of years, this has produced huge quantities of carbonate rocks.
Ultimately, most of the CO
2 emitted by human activities will dissolve in the ocean  however, the rate at which the ocean will take it up in the future is less certain. Even if equilibrium is reached, including dissolution of carbonate minerals, the increased concentration of bicarbonate and decreased or unchanged concentration of carbonate ion will give rise to a higher concentration of un-ionized carbonic acid and dissolved CO
2 . This higher concentration in the seas, along with higher temperatures, would mean a higher equilibrium concentration of CO
2 in the air.  
Carbon dioxide has unique long-term effects on climate change that are nearly "irreversible" for a thousand years after emissions stop (zero further emissions). The greenhouse gases methane and nitrous oxide do not persist over time in the same way as carbon dioxide. Even if human carbon dioxide emissions were to completely cease, atmospheric temperatures are not expected to decrease significantly in the short term. This is because the air temperature is determined by a balance between heating, due to greenhouse gases, and cooling due to heat transfer to the ocean. If emissions were to stop, CO
2 levels and the heating effect would slowly decrease, but simultaneously the cooling due to heat transfer would diminish (because sea temperatures would get closer to the air temperature), with the result that the air temperature would decrease only slowly. Sea temperatures would continue to rise, causing thermal expansion and some sea level rise.  Lowering global temperatures more rapidly would require carbon sequestration or geoengineering.
Carbon moves between the atmosphere, vegetation (dead and alive), the soil, the surface layer of the ocean, and the deep ocean. A detailed model has been developed by Fortunat Joos in Bern and colleagues, called the Bern model.  A simpler model based on it gives the fraction of CO
2 remaining in the atmosphere as a function of the number of years after it is emitted into the atmosphere: 
According to this model, 21.7% of the carbon dioxide released into the air stays there forever, but of course this is not true if carbon-containing material is removed from the cycle (and stored) in ways that are not operative at present (artificial sequestration).
2 absorption and release is always happening as a result of natural processes, the recent rise in CO
2 levels in the atmosphere is known to be mainly due to human (anthropogenic) activity.  There are four ways human activity, especially fossil fuel burning, is known to have caused the rapid increase in atmospheric CO
2 over the last few centuries:
- Various national statistics accounting for fossil fuel consumption, combined with knowledge of how much atmospheric CO
2 is produced per unit of fossil fuel (e.g. liter of gasoline). 
- By examining the ratio of various carbon isotopes in the atmosphere.  The burning of long-buried fossil fuels releases CO
2 containing carbon of different isotopic ratios to those of living plants, enabling distinction between natural and human-caused contributions to CO
- Higher atmospheric CO
2 concentrations in the Northern Hemisphere, where most of the world's population lives (and emissions originate from), compared to the southern hemisphere. This difference has increased as anthropogenic emissions have increased. 
- Atmospheric O2 levels are decreasing in Earth's atmosphere as it reacts with the carbon in fossil fuels to form CO
2 . 
Burning fossil fuels such as coal, petroleum, and natural gas is the leading cause of increased anthropogenic CO
2 deforestation is the second major cause. In 2010, 9.14 gigatonnes of carbon (GtC, equivalent to 33.5 gigatonnes of CO
2 or about 4.3 ppm in Earth's atmosphere) were released from fossil fuels and cement production worldwide, compared to 6.15 GtC in 1990.  In addition, land use change contributed 0.87 GtC in 2010, compared to 1.45 GtC in 1990.  In 1997, human-caused Indonesian peat fires were estimated to have released between 13% and 40% of the average annual global carbon emissions caused by the burning of fossil fuels.    In the period 1751 to 1900, about 12 GtC were released as CO
2 to the atmosphere from burning of fossil fuels, whereas from 1901 to 2013 the figure was about 380 GtC. 
The Integrated Carbon Observation System (ICOS) continuously releases data about CO
2 emissions, budget and concentration at individual observation stations.
|Year||Fossil fuels |
|Land use |
Anthropogenic carbon emissions exceed the amount that can be taken up or balanced out by natural sinks.  As a result, carbon dioxide has gradually accumulated in the atmosphere, and as of 2019 [update] , its concentration is almost 48% above pre-industrial levels.  Various techniques have been proposed for removing excess carbon dioxide from the atmosphere (see Carbon sink#Artificial sequestration). Currently about half of the carbon dioxide released from the burning of fossil fuels is not absorbed by vegetation and the oceans and remains in the atmosphere. 
Global fossil carbon emissions 1800–2014
False-color image of smoke and ozone pollution from Indonesian fires, 1997
2 flux in the northern hemisphere winter (NOAA Carbon Tracker)
2 flux in the northern hemisphere summer (NOAA Carbon Tracker)
The first reproducibly accurate measurements of atmospheric CO2 were from flask sample measurements made by Dave Keeling at Caltech in the 1950s.  A few years later in March 1958 the first ongoing measurements were started by Keeling at Mauna Loa. Measurements at Mauna Loa have been ongoing since then. Now measurements are made at many sites globally. Additional measurement techniques are also used as well. Many measurement sites are part of larger global networks. Global network data are often made publicly available on the conditions of proper acknowledgment according to the respective data user policies.
There are several surface measurement (including flasks and continuous in situ) networks including NOAA/ERSL,  WDCGG,  and RAMCES.  The NOAA/ESRL Baseline Observatory Network, and the Scripps Institution of Oceanography Network  data are hosted at the CDIAC at ORNL. The World Data Centre for Greenhouse Gases (WDCGG), part of GAW, data are hosted by the JMA. The Reseau Atmospherique de Mesure des Composes an Effet de Serre database (RAMCES) is part of IPSL.
From these measurements, further products are made which integrate data from the various sources. These products also address issues such as data discontinuity and sparseness. GLOBALVIEW-CO2 is one of these products. 
Ongoing ground-based total column measurements began more recently. Column measurements typically refer to an averaged column amount denoted XCO2, rather than a surface only measurement. These measurements are made by the TCCON. These data are also hosted on the CDIAC, and made publicly available according to the data use policy. 
Satellite measurements are also a recent addition to atmospheric XCO2 measurements. SCIAMACHY aboard ESA's ENVISAT made global column XCO2 measurements from 2002 to 2012. AIRS aboard NASA's Aqua satellite makes global XCO2 measurements and was launched shortly after ENVISAT in 2012. More recent satellites have significantly improved the data density and precision of global measurements. Newer missions have higher spectral and spatial resolutions. JAXA's GOSAT was the first dedicated GHG monitoring satellite to successfully achieve orbit in 2009. NASA's OCO-2 launched in 2014 was the second. Various other satellites missions to measure atmospheric XCO2 are planned.
Life [ edit ]
He was according to Cicero (ad Fam. ix. 21) the father of the Carbo of the same name, who was thrice consul, whereas this latter is called by Velleius Paterculus (II 26) a brother of Gaius Papirius Carbo Arvina. This difficulty may be solved by supposing that the word frater in Velleius is equivalent to frater patruelis or cousin. (Perizon., Animadv. Hist. p.㻠.)
During his consulship, he was ordered by the Senate to take legions to defend the Alps from the migration of the Cimbri. Ώ] There, he shadowed the Germanic tribe and ambushed them near Noreia. At the ensuing Battle of Noreia, although Carbo held the advantage in terrain and surprise, his forces were overwhelmed by the sheer magnitude of Cimbrian warriors, ΐ] and disastrously defeated. Α] The Cimbri, while smashing the Roman army, did not advance into Italy, seemingly looking for some place to settle. ΐ]
He was afterwards accused by Marcus Antonius for provoking and then losing the Battle of Noreia. Β] Securing a conviction, Carbo committed suicide rather than depart for exile, Γ] taking a solution of vitriol (atramentum sutorium, Cic., ad Fam. IX 21 Liv., Epit. 63.).
A member of the plebeian gen Norbani and a novus homo, Gaius Norbanus first came to prominence when he was elected one of the plebeian tribunes for 103 BC. He achieved notoriety for his prosecution of Quintus Servilius Caepio, where he accused Servilius Caepio of incompetence and dereliction of duty at the catastrophic defeat of the Roman armies by the Cimbri at the Battle of Arausio in 105 BC.  [a] At the concilium plebis where Servilius Caepio was tried, two tribunes attempted to veto proceedings, but were driven off by force.  Although the Senate vigorously tried to obtain his acquittal and he was defended by Lucius Licinius Crassus, Norbanus managed to secure Caepio’s conviction. Caepio was forced into exile to Smyrna, while his fortune was confiscated.
In 101 BC, Norbanus served as quaestor under Marcus Antonius, grandfather of the triumvir Mark Antony, in his campaign against the pirates in Cilicia.  In 94 BC, Norbanus was accused of minuta maiestas (treason) under the Lex Appuleia by Publius Sulpicius Rufus on account of the disturbances that had taken place at the trial of Caepio, but the eloquence of Marcus Antonius secured his acquittal.  
This was followed by his election as Praetor in 89 BC, and his appointment as governor of Sicily. He kept the peace in his province, defending it against the Italian socii during the Social War.  He managed to capture Rhegium from the Samnites in 88 BC.  
During the civil war between Gaius Marius and Lucius Cornelius Sulla he sided with Marius.  He was elected consul for 83 BC  at Mount Tifata, near Capua, he intercepted Sulla, who had returned to Italy from Greece. Sulla sent over some emissaries to discuss coming to terms with Norbanus, but they were thrown out when it became apparent that they were trying to suborn Norbanus’ men, who were mostly raw recruits.  Although Norbanus was helped by Quintus Sertorius, they were defeated by Sulla at the Battle of Mount Tifata,  losing around 6,000 men in the process. [ citation needed ] He managed to regroup his shattered army at Capua,  whereupon he eventually retreated to Cisalpine Gaul.  He and Gnaeus Papirius Carbo were defeated by Quintus Caecilius Metellus Pius at Faventia.  Norbanus was betrayed by one of his legates, Publius Tullius Albinovanus, who murdered many of Norbanus’ principal officers after inviting them to dinner  before surrendering Ariminium to Metellus Pius. 
Norbanus himself did not attend Albinovanus' invitation, and he managed to evade capture, fleeing to Rhodes.  After proscription by Sulla, he committed suicide in the middle of a market-place, while the leading citizens of Rhodes were debating whether to hand him over to Sulla's men.  
Lucius Cornelius Cinna
From Wikipedia, the free encyclopedia
Lucius Cornelius Cinna (d. 84 BC) was a four-time consul of the Roman Republic, serving consecutive terms from 87 to 84 BC, and a member of the ancient Roman Cinna family of the Cornelii gens. Cinna supported Gaius Marius in Marius's contest with Sulla. After serving in the war with the Marsi as praetorian legate, he was elected consul in 87 BC.
Breaking the oath he had sworn to Sulla that he would not attempt any revolution in the republic, Cinna allied himself with Marius, raised an army of Italians, and took possession of the city. Soon after his triumphant entry and the massacre of the friends of Sulla, by which he had satisfied his vengeance, Marius died. Lucius Valerius Flaccus was to became Cinna's colleague in 85 BC but was murdered by Gaius Flavius Fimbria. Gnaeus Papirius Carbo became Cinna's colleague in Flaccus' stead. In 84 BC, Cinna, during his fourth year as consul, was forced to advance against Sulla but while embarking his troops for Liburnia, Illyricum, he was killed in a mutiny (App. BC iv.1.77-78).
His youngest daughter, Cornelia, married Julius Caesar and died young after bearing him his only legitimate child, a Julia Caesaris who married Gnaeus Pompeius Magnus. His son, also named Lucius Cornelius Cinna, was a praetor who sided with the murderers of Julius Caesar and publicly extolled their action.
^ Latin: L·CORNELIVS·L·F·L·N·CINNA English: "Lucius Cornelius Cinna, son of Lucius, grandson of Lucius".
This article incorporates text from the Encyclopædia Britannica Eleventh Edition, a publication now in the public domain.
Lucius Cornelius Sulla and Quintus Pompeius Rufus Consul of the Roman Republic
with Gnaeus Octavius
87 BC Succeeded by
Lucius Cornelius Cinna and Gaius Marius
(suffect: Lucius Valerius Flaccus)
Lucius Cornelius Cinna and Gnaeus Octavius Consul of the Roman Republic
with Gaius Marius
(Suffect: Lucius Valerius Flaccus)
86 BC Succeeded by
Lucius Cornelius Cinna and Gnaeus Papirius Carbo
Lucius Cornelius Cinna and Gaius Marius
(Suffect: Lucius Valerius Flaccus) Consul of the Roman Republic
Gnaeus Papirius Carbo
85 BC Succeeded by
Lucius Cornelius Cinna and Gnaeus Papirius Carbo
Lucius Cornelius Cinna and Gnaeus Papirius Carbo Consul of the Roman Republic
Gnaeus Papirius Carbo
84 BC Succeeded by
Lucius Cornelius Scipio Asiaticus Asiagenus and Gaius Norbanus