Evidence found in the fossil record indicates that in the distant past, the earth's climate was very different than it is today. There have also been substantial climatic fluctuations within the last several centuries, too recently for the changes to be reflected in the fossil record. Since these changes are important to understanding potential future climate change, scientists have developed methods to study the climate of the recent past.
Although human-recorded weather records cover only the last few hundred years or so, paleoclimatologists and paleobotanists have found ways of identifying the kinds of plants that grew in a given area, from which they can infer the kind of climate that must have prevailed. Because plants are generally distributed across the landscape based on temperature and precipitation patterns, plant communities change as these climatic factors change. By knowing the conditions that plants preferred, scientists can make general conclusions about the past climate.
How do paleobotanists map plant distribution over time? One way is to study the pollen left in lake sediments by wind-pollinated plants that once grew in the lake's vicinity. Sediment in the bottom of lakes is ideal for determining pollen changes over time because it tends to be laid down in annual layers (much like trees grow annual rings). Each layer traps the pollen that sank into the lake or was carried into it by stream flow that year.
To look at the "pollen history" of a lake, scientists collect long cores of lake sediment, using tubes approximately 5 centimeters (cm) in diameter. The cores can be 10 m long or longer, depending upon the age of the lake and amount of sediment that's been deposited. The removed core is sampled every 10 to 20 cm and washed in solutions of very strong, corrosive chemicals, such as potassium hydroxide, hydrochloric acid, and hydrogen fluoride. This harsh process removes the organic and mineral particles in the sample except for the pollen, which is composed of some of the most chemically resistant organic compounds in nature. Microscope slides are made of the remaining pollen and examined to count and identify the pollen grains.
Because every plant species has a distinctive pollen shape, botanists can identify from which plant the pollen came. Through pollen analysis, botanists can estimate the composition of a lake area by comparing the relative amount of pollen each species contributes to the whole pollen sample. Carbon dating of the lake sediment cores gives an approximate age of the sample.
Scientists can infer the climate of the layer being studied by relating it to the current climatic preferences of the same plants. For example, they can infer that a sediment layer with large amounts of western red cedar pollen was deposited during a cool, wet climatic period, because those are the current conditions most conducive to the growth of that species.
Why are scientists who study climate change interested in past climates? First, by examining the pattern of plant changes over time, they can determine how long it took for plant species to migrate into or out of a given area due to natural processes of climate change. This information makes it easier to predict the speed with which plant communities might change in response to future climate change. Second, by determining the kinds of plants that existed in an area when the climate was warmer than at present, scientists can more accurately predict which plants will be most likely to thrive if the climate warms again.
The Paleoclimate of Battle Ground Lake, Washington
The research site is located 30 km north of the Columbia River, in Clark County Washington, near the town of Battle Ground. This description was provided by Dr. Cathy Whitlock.
The lake has been in existence for at least the last 20,000 years and has continuously accumulated sediments through most of that time. Trapped in the sediments are pollen grains from the plants that grew in the general vicinity of the lake at the time the sediments were deposited. By examining the pollen in different layers of sediment from the bottom layer to the top, we can reconstruct the vegetation changes that have occurred in the area during the lake's existence. Because we know something about the climatic conditions that the plants needed to survive, we can use the vegetation data to reconstruct the past climate in the area for the entire 20,000-year period.
Many layers have been identified by paleoclimatologists. For the sake of simplicity, we will combine these into five major layers. The age of each layer has been established by radiocarbon dating and by reference to volcanic ash layers of known age from Mt. St. Helens and from the explosion of Mt. Mazama (now Crater Lake in Oregon).
4,500 years before present (ybp) - Present
A cooler and moister period than the previous one. The dry-land vegetation is replaced by the extensive closed coniferous forests seen today, with hemlock and western red cedar dominating the areas of forest undisturbed by logging.
9,500 - 4,500 ybp
The climate continues to warm with mild, moist winters and warm, dry summers predominating. The forests of the previous period (which needed cooler, moister conditions) disappear to be replaced by more drought-adapted mixed oak, Douglas fir, and a dry meadowland community. Today, such vegetation is typical of areas of the Willamette Valley of Oregon that have escaped cultivation.
11,200 - 9,500 ybp
The warming continues and the first occurrence of "modern," temperate coniferous forest is found in this period as Douglas fir, alder, and grand fir dominate in forests not unlike those that occur today. The climate is similar to today's climate as well.
15,000 - 11,200 ybp
Glaciers have begun to recede as the climate starts a warming trend. Although still cold in comparison to the present climate, the warming has progressed enough to allow more extensive forests of lodgepole pine, Engelmann spruce, and grand fir to replace the tundra vegetation in an open woodland setting. Further north in the northern and central Puget Lowland, the glacial recession has opened up many new areas to plant colonization, and lodgepole pine has invaded these new areas.
20,000 - 15,000 ybp
Glacial maximum, with nearly a vertical mile of ice over the site of Seattle, and the continental glaciers extending south of the present site of Olympia. An alpine glacier from Mt. St. Helens extended down the Lewis River Valley to within 30 km of the lake site. The lake area climate was cold, with a short growing season. The landscape resembled an arctic/alpine tundra, with alpine grasses/sedges, low woody shrubs, and scattered tree islands of cold-tolerant Engelmann spruce and lodgepole pine dominating the meadows.
Reference: Barnosky, C. W., 1985. Late quaternary vegetation near Battle Ground Lake, southern Puget Trough, Washington. Geological Society of America Bull., 96, 263 - 271.
The Paleoclimate of Blackhawk, Colorado
The research site simulated in this activity is the Eiven Jacobson farm outside the town of Blackhawk, Colorado. It is located on the Peak to Peak Highway at an elevation of 9002 feet.
In a valley on the farm, a peat bog developed over the centuries. Through carbon-14 dating of the sediment layer and pollen samples, the paleoclimate of this area of Colorado has been established. The peat bog and soils underneath it have been in existence for eons and have accumulated sediments over time. Trapped in these sediments are pollen grains from a variety of plants that grew in the area at the time the sediments were deposited. By examining the sediments from the bottom to top (oldest to youngest), we can reconstruct the vegetation changes that occurred in the farm's area during the last several thousand years. Because we know something of the climatic conditions that these plants need to survive, we can use the vegetation data to reconstruct the past climate in this area for the last 10,000 years. As climate changes with time, so do the plant communities. Plant communities will migrate up the mountains during the warming periods and fall back down again as the climate cools. The tree line changes in conjunction with this shift, perhaps helping us understand why there are ancient bristlecone pines on Mt. Evans (elevation 14,000+ feet).
150 Years Before Present (ybp) - Present
As our temperatures warm from the Little Ice Age, the plants change as well, back to those that thrive in warmer climates. Today at approximately 9000 feet, we find ponderosa pines, meadow grasses, wildflowers, and aspens, which are all indicative of the milder climate we are experiencing.
650 - 150 ybp
The term "Little Ice Age" gives us an idea of a change that began to happen climatically at this time. Gone were the warm days of the Medieval Warming Period and the big chill set in; cooler temperatures were the norm. Once again the Engelmann spruce and limber, lodgepole, and bristlecone pines dotted the landscape.
1,500 - 650 ybp
This period is termed the "Medieval Warming Period." No longer do the spruces and cold-tolerant plants dominate the landscapes. The vegetation is also shifting with the change in temperatures. Now the landscapes primarily consist of ponderosa pines, Douglas fir, meadow grasses, and wildflowers.
3,500 - 1,500 ybp
A cooler and moister period succeeds the past warmer climate. The predominant vegetation species are Engelmann spruces, limber, lodgepole, and bristlecone pines, aspen, and wet peat plants, such as sedges, willows, and mosses. At about 2,000 ybp, the peat from the Jacobson's peat bog began to develop and grow in this cooler, wetter climate.
8,000 - 3,500 ybp
This was a warmer era, with the vegetation dominated by Douglas fir, ponderosa pine, aspen, meadow grasses, and wildflowers, similar to what we see now on the Jacobson farm. These species tend to grow best under temperate, somewhat moist conditions. Forest fires were also quite prevalent during this time.
10,000 - 8,000 ybp
The period right after the last glacier was a very cold time with gradual warming. The cold temperatures at the end of the Pleistocene period were giving way to the warming trends of the Holocene. The era was characterized by a very short growing season. The landscape resembled an arctic/alpine tundra, with the meadows dominated by alpine grasses, daisies, alpine sage, and sedges. Scatter trees, the cold-tolerant Engelmann spruce, some willows, and aspens began to appear toward the end of this period in scattered tree islands.
This information was provided by the Science Discovery Program at the University of Colorado - Boulder.