A Brief History of Manchuria

A Brief History of Manchuria Manchuria is the region of northeastern China that now covers the provinces of Heilongjiang, Jilin, and Liaoning. Some geographers also include northeastern Inner Mongolia, as well. Manchuria has a long history of conquering and being conquered by its southwestern neighbor, China. Naming Controversy The name Manchuria is controversial. It comes from a European adoption of the Japanese name Manshu, which the Japanese began to use in the nineteenth century. Imperial Japan wanted to pry that area free from Chinese influence. Eventually, in the early 20th century, Japan would annex the region outright.   The so-called Manchu people themselves, as well as the Chinese, did not use this term, and it is considered problematic, given its connections with Japanese imperialism. Chinese sources generally call it the Northeast or the Three Northeast Provinces. Historically, it is also known as Guandong, meaning east of the pass. Nonetheless, Manchuria is still considered to be the standard name for northeastern China in the English language.   The Manchu People Manchuria is the traditional land of the Manchu  (formerly called the Jurchen), the Xianbei (Mongols), and the  Khitan  peoples. It also has long-standing populations of Korean and Hui Muslim people.  Ã¢â‚¬â€¹In total, the Chinese central government recognizes 50 ethnic minority groups in Manchuria.  Today, it is home to more than 107 million people; however, the vast majority of them are ethnic Han Chinese. During the late Qing Dynasty (19th and early 20th centuries), the ethnic-Manchu Qing emperors encouraged their Han Chinese subjects to settle the area that was the Manchu homeland. They took this surprising step to counter Russian expansionism in the region. The mass migration of Han Chinese is called the  Chuang Guandong, or the venture into the east of the pass. Manchuria's History The first empire to unite nearly all of Manchuria was the Liao Dynasty (907 - 1125 CE). The Great Liao is also known as the Khitan Empire, which took advantage of the collapse of Tang China to spread its territory into China proper, as well. The Manchuria-based Khitan Empire was powerful enough to demand and receive tribute from Song China and also from the Goryeo Kingdom in Korea. Another Liao tributary people, the Jurchen, overthrew the Liao Dynasty in 1125 and formed the Jin Dynasty. The Jin would go on to rule much of northern China and Mongolia from 1115 to 1234 CE. They were conquered by the rising Mongol Empire under Genghis Khan. After the Mongols Yuan Dynasty in China fell in 1368, a new ethnic Han Chinese dynasty arose called the Ming. The Ming were able to assert control over Manchuria and forced the Jurchens and other local people to pay tribute to them. However, when unrest broke out in the late Ming era, the emperors invited Jurchen/Manchu mercenaries to fight in the civil war.  Instead of defending the Ming, the Manchus conquered all of China in 1644. Their new empire, ruled by the Qing Dynasty, would be the last Imperial Chinese Dynasty  and lasted until 1911. After the fall of the Qing Dynasty, Manchuria was conquered by the Japanese, who renamed it Manchukuo. It was a puppet empire, headed by the former Last Emperor of China, Puyi. Japan launched its invasion of China proper from Manchukuo; it would hold on to Manchuria until the end of World War II. When the Chinese Civil War ended in a victory for the communists in 1949, the new Peoples Republic of China took control of Manchuria. It has remained a part of China ever since.

Radiocarbon Dating - Reliable but Misunderstood

Radiocarbon Dating - Reliable but Misunderstood Radiocarbon dating is one of the best known archaeological dating techniques available to scientists, and the many people in the general public have at least heard of it. But there are many misconceptions about how radiocarbon works and how reliable a technique it is. Radiocarbon dating was invented in the 1950s by the American chemist Willard F. Libby and a few of his students at the University of Chicago: in 1960, he won a Nobel Prize in Chemistry for the invention. It was the first absolute scientific method ever invented: that is to say, the technique was the first to allow a researcher to determine how long ago an organic object died, whether it is in context or not. Shy of a date stamp on an object, it is still the best and most accurate of dating techniques devised. How Does Radiocarbon Work? All living things exchange the gas Carbon 14 (C14) with the atmosphere around them- animals and plants exchange Carbon 14 with the atmosphere, fish and corals exchange carbon with dissolved C14 in the water. Throughout the life of an animal or plant, the amount of C14 is perfectly balanced with that of its surroundings. When an organism dies, that equilibrium is broken. The C14 in a dead organism slowly decays at a known rate: its half life. The half-life of an isotope like C14 is the time it takes for half of it to decay away: in C14, every 5,730 years, half of it is gone. So, if you measure the amount of C14 in a dead organism, you can figure out how long ago it stopped exchanging carbon with its atmosphere. Given relatively pristine circumstances, a radiocarbon lab can measure the amount of radiocarbon accurately in a dead organism for as long as 50,000 years ago; after that, theres not enough C14 left to measure. Tree Rings and Radiocarbon There is a problem, however. Carbon in the atmosphere fluctuates with the strength of earths magnetic field and solar activity. You have to know what the atmospheric carbon level (the radiocarbon reservoir) was like at the time of an organisms death, in order to be able to calculate how much time has passed since the organism died. What you need is a ruler, a reliable map to the reservoir: in other words, an organic set of objects that you can securely pin a date on, measure its C14 content and thus establish the baseline reservoir in a given year. Fortunately, we do have an organic object that tracks carbon in the atmosphere on a yearly basis: tree rings. Trees maintain carbon 14 equilibrium in their growth rings- and trees produce a ring for every year they are alive. Although we dont have any 50,000-year-old trees, we do have overlapping tree ring sets back to 12,594 years. So, in other words, we have a pretty solid way to calibrate raw radiocarbon dates for the most recent 12,594 years of our planets past. But before that, only fragmentary data is available, making it very difficult to definitively date anything older than 13,000 years. Reliable estimates are possible, but with large /- factors. The Search for Calibrations As you might imagine, scientists have been attempting to discover other organic objects that can be dated securely steadily since Libbys discovery. Other organic data sets examined have included varves (layers in sedimentary rock which were laid down annually and contain organic materials, deep ocean corals, speleothems (cave deposits), and volcanic tephras; but there are problems with each of these methods. Cave deposits and varves have the potential to include old soil carbon, and there are as-yet unresolved issues with fluctuating amounts of C14 in ocean corals. Beginning in the 1990s, a coalition of researchers led by Paula J. Reimer of the CHRONO Centre for Climate, the Environment and Chronology, at Queens University Belfast, began building an extensive dataset and calibration tool that they first called CALIB. Since that time, CALIB, now renamed IntCal, has been refined several timesas of this writing (January 2017), the program is now called IntCal13. IntCal combines and reinforces data from tree-rings, ice-cores, tephra, corals, and speleothems to come up with a significantly improved calibration set for c14 dates between 12,000 and 50,000 years ago. The latest curves were ratified at the 21st International Radiocarbon Conference in July of 2012. Lake Suigetsu, Japan Within the last few years, a new potential source for further refining radiocarbon curves is Lake Suigetsu in Japan. Lake Suigetsus annually formed sediments hold detailed information about environmental changes over the past 50,000 years, which radiocarbon specialist PJ Reimer believes will be as good as, and perhaps better than, samples cores from the Greenland Ice Sheet. Researchers Bronk-Ramsay et al. report 808 AMS dates based on sediment varves measured by three different radiocarbon laboratories. The dates and corresponding environmental changes promise to make direct correlations between other key climate records, allowing researchers such as Reimer to finely calibrate radiocarbon dates between 12,500 to the practical limit of c14 dating of 52,800. Constants and Limits Reimer and colleagues point out that IntCal13 is just the latest in calibration sets, and further refinements are to be expected. For example, in IntCal09s calibration, they discovered evidence that during the Younger Dryas (12,550-12,900 cal BP), there was a shutdown or at least a steep reduction of the North Atlantic Deep Water formation, which was surely a reflection of climate change; they had to throw out data for that period from the North Atlantic and use a different dataset. We should see some interesting results in the very near future. Sources and Further Information Bronk Ramsey C, Staff RA, Bryant CL, Brock F, Kitagawa H, Van der Plicht J, Schlolaut G, Marshall MH, Brauer A, Lamb HF et al. 2012. A complete terrestrial radiocarbon record for 11.2 to 52.8 kyr B.P. Science 338:370-374.Reimer PJ. 2012. Atmospheric science. Refining the radiocarbon time scale. Science 338(6105):337-338.Reimer PJ, Bard E, Bayliss A, Beck JW, Blackwell PG, Bronk Ramsey C, Buck CE, Cheng H, Edwards RL, Friedrich M et al. . 2013. IntCal13 and Marine13 Radiocarbon Age Calibration Curves 0–50,000 Years cal BP. Radiocarbon 55(4):1869–1887.Reimer P, Baillie M, Bard E, Bayliss A, Beck J, Blackwell PG, Bronk Ramsey C, Buck C, Burr G, Edwards R et al. 2009. IntCal09 and Marine09 radiocarbon age calibration curves, 0-50,000 years cal BP. Radiocarbon 51(4):1111-1150.Stuiver M, and Reimer PJ. 1993. Extended C14 data base and revised Calib 3.0 c14 age calibration program. Radiocarbon 35(1):215-230.