hypothesis of water cycle

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water cycle

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• NASA - Global Precipitation Measurement - The Water Cycle
• U.S. Geological Survey - The Water Cycle
• Chemistry Libretexts - Water Cycle
• Northwest River Forecast Center - The Water Cycle
• NeoK12 - Educational Videos and Games for School Kids - Water Cycle
• Pennsylvania State University - Department of Energy and Mineral Engineering - Understanding water cycle
• UCAR Center for Science Education - The Water Cycle
• water cycle - Children's Encyclopedia (Ages 8-11)
• water cycle - Student Encyclopedia (Ages 11 and up)

• What are the main stages of the water cycle?
• How does evaporation contribute to the water cycle?
• What role do clouds play in the water cycle?
• How does precipitation occur in the water cycle?
• What is the importance of groundwater in the water cycle?
• How does human activity impact the natural water cycle?
• What is transpiration and how does it relate to the water cycle?
• How does the water cycle affect climate and weather patterns?
• What are aquifers and how do they fit into the water cycle?

water cycle , cycle that involves the continuous circulation of water in the Earth - atmosphere system. Of the many processes involved in the water cycle, the most important are evaporation , transpiration , condensation , precipitation , and runoff . Although the total amount of water within the cycle remains essentially constant, its distribution among the various processes is continually changing.

A brief treatment of the water cycle follows. For full treatment, see hydrosphere: The water cycle .

Evaporation , one of the major processes in the cycle, is the transfer of water from the surface of the Earth to the atmosphere. By evaporation, water in the liquid state is transferred to the gaseous , or vapor, state. This transfer occurs when some molecules in a water mass have attained sufficient kinetic energy to eject themselves from the water surface. The main factors affecting evaporation are temperature , humidity , wind speed, and solar radiation . The direct measurement of evaporation, though desirable, is difficult and possible only at point locations. The principal source of water vapor is the oceans , but evaporation also occurs in soils , snow , and ice . Evaporation from snow and ice, the direct conversion from solid to vapor, is known as sublimation. Transpiration is the evaporation of water through minute pores, or stomata, in the leaves of plants . For practical purposes, transpiration and the evaporation from all water, soils, snow, ice, vegetation, and other surfaces are lumped together and called evapotranspiration , or total evaporation.

Water vapor is the primary form of atmospheric moisture. Although its storage in the atmosphere is comparatively small, water vapor is extremely important in forming the moisture supply for dew , frost , fog , clouds , and precipitation. Practically all water vapour in the atmosphere is confined to the troposphere (the region below 6 to 8 miles [10 to 13 km] altitude).

The transition process from the vapor state to the liquid state is called condensation . Condensation may take place as soon as the air contains more water vapour than it can receive from a free water surface through evaporation at the prevailing temperature. This condition occurs as the consequence of either cooling or the mixing of air masses of different temperatures. By condensation, water vapor in the atmosphere is released to form precipitation .

Precipitation that falls to the Earth is distributed in four main ways: some is returned to the atmosphere by evaporation, some may be intercepted by vegetation and then evaporated from the surface of leaves , some percolates into the soil by infiltration, and the remainder flows directly as surface runoff into the sea. Some of the infiltrated precipitation may later percolate into streams as groundwater runoff. Direct measurement of runoff is made by stream gauges and plotted against time on hydrographs.

Most groundwater is derived from precipitation that has percolated through the soil. Groundwater flow rates, compared with those of surface water, are very slow and variable, ranging from a few millimeters to a few meters a day. Groundwater movement is studied by tracer techniques and remote sensing.

Ice also plays a role in the water cycle. Ice and snow on the Earth’s surface occur in various forms such as frost, sea ice , and glacier ice. When soil moisture freezes, ice also occurs beneath the Earth’s surface, forming permafrost in tundra climates . About 18,000 years ago glaciers and ice caps covered approximately one-third of the Earth’s land surface. Today about 12 percent of the land surface remains covered by ice masses.

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When and how was the water cycle discovered?

When and how was the water cycle discovered? Did people, like ancient Greek philosophers, have any correct ideas on the water cycle? Was its discovery more of a recent thing?

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• 2 $\begingroup$ Some argue that the water cycle was completely understood by Hebrew scholars as evidenced by the text fom the Hebrew bible dated as early as the 10th century BCE. $\endgroup$ –  nwr Commented Feb 9, 2020 at 20:22
• 2 $\begingroup$ " The first published thinker to assert that rainfall alone was sufficient for the maintenance of rivers was Bernard Palissy (1580 CE), who is often credited as the "discoverer" of the modern theory of the water cycle. Palissy's theories were not tested scientifically until 1674, in a study commonly attributed to Pierre Perrault. " $\endgroup$ –  Conifold Commented Feb 10, 2020 at 8:18
• $\begingroup$ It was understood in a general way in the ancient world. $\endgroup$ –  Mozibur Ullah Commented Dec 5, 2020 at 17:30
• $\begingroup$ This article discusses this topic of the water cycle. I recommend giving it a read: Science and the Bible $\endgroup$ –  Peter Peterson Commented Apr 14, 2021 at 8:49

In Aristotles Meteorology , we have:

Now, the sun, moving as it does, sets up processes of change and becoming and decay, and by it's agency the finest and the sweetest water is carried up and is dissolved into vapour and rises to the upper region, where it is condensed again by the cold and so returns the earth.

And he notes this again in his Physics that:

Zeus does not send the rain in order to make the corn grow: it comes of neccessity. The stuff which has been drawn up is bound to cool, and having cooled, turns to water and comes down. It is merely concurrent that this having happened, the corn grows.

Hence, the hydrological or water cycle, at least in Europe, was known by Aristotles time, and so by 350 BCE.

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Water Cycle

What is the water cycle.

Water cycle, also known as the hydrologic cycle, involves a series of stages that show the continuous movement and interchange of water between its three phases – solid, liquid, and gas, in the earth’s atmosphere. The sun acts as the primary source of energy that powers   the   water cycle on earth. Bernard Palissy discovered the modern theory of the water cycle in 1580 CE.

Steps of the Water Cycle: How does it Work

1. Change from Liquid to Gaseous Phase – Evaporation and Transpiration

The heat of the sun causes water from the surface of water bodies such as oceans, streams, and lakes to evaporate into water vapor in the atmosphere. Plants also contribute to the water cycle when water gets evaporated from the aerial parts of the plant , such as leaves and stems by the process of transpiration.

2. Change from Solid to Gaseous Phase – Sublimation

Due to dry winds, low humidity, and low air pressure, snow present on the mountains change directly into water vapor, bypassing the liquid phase by a process known as sublimation.

3. Change from Gaseous to Liquid Phase – Condensation

The invisible water vapor formed through evaporation, transpiration, and sublimation rises through the atmosphere, while cool air rushes to take its place. This is the process of condensation that allows water vapor to transform back into liquid, which is then stored in the form of clouds.

Sometimes, a sudden drop in atmospheric temperature helps the water vapors to condense into tiny droplets of water that remain suspended in the air. These suspended water droplets get mixed with bits of dust in the air, resulting in fog.

4. Change from Gaseous to Liquid and Solid Phase – Precipitation and Deposition         

Wind movements cause the water-laden clouds   to collide and fall back on the earth’s surface through precipitation, simply known as rain. The water that evaporated in the first stage thus returns into different water bodies on the earth’s surface, including the ocean, rivers, ponds, and lakes. In regions with extremely cold climate with sub-zero temperatures, the water vapor changes directly into frost and snow bypassing the liquid phase, causing snowfall in high altitudes by a process known as the deposition. 

5. Return of the water back into the underground reserve – Runoff, Infiltration, Percolation, and Collection

The water that falls back on the earth’s surface moves between the layers of soil and rocks and is accumulated as the underground water reserves known as aquifers. This process is further assisted by earthquakes, which help the underground water to reach the mantle of the earth. Some amount of precipitated water flows down the sides of mountains and hills to reach the water bodies, which again evaporates into the atmosphere. During volcanic eruptions, the underground water returns to the surface of the earth, where it mixes with the surface water bodies in order to continue the cycle.

Video: Water Cycle Explained

Why is the water cycle important.

The most crucial and direct impacts of the above process on earth include:

• Making fresh water available to plants and animals, including humans, by purifying the groundwater on earth. During the water cycle, the water evaporates, leaving behind all the sediments and other dust particles. Similarly, for the sustenance of marine life, the saline range of all salt water bodies is kept within a certain permissible limit through infiltration. 
• Allowing even distribution of water on all surfaces of the earth. Water is temporarily stored as clouds in the atmosphere, whereas surface water bodies such as rivers and oceans, together with underground water, form the major permanent water reserves. 
• Causing a cooling effect on earth due to evaporation of water from surface water bodies, which help to form clouds that eventually precipitate down in the form of rain. This way water cycle affects the weather and climate of the earth.
• Ensuring some other biogeochemical cycles , including those concerning oxygen and phosphorus, to continue in nature.
• Cleaning the atmosphere by taking-away dust particles, shoot, and bacteria , thus acting as a means to purify the air we breathe.

Human Impact on Water Cycle

Human activities adversely affect the water cycle in the two following ways:

a) Deforestation : Plants play an important role in the water cycle by preventing soil erosion and thus helps to increase the groundwater level of the earth. Also, plants contribute by absorbing water from the soil, which is then released back to the atmosphere during transpiration. Deforestation adversely affects both the above processes, thus breaking the flow of the water cycle.

b) Pollution : Burning of fossil fuels acts as the major source of air pollution releasing toxic gases into the atmosphere, leading to the formation of smog and acid rain . Water from farmlands run off to the nearest water bodies carrying chemicals such as insecticides and pesticides along with them, thus causing water pollution. The presence of excessive contaminants in the atmosphere and water bodies decreases the evaporation and condensation on earth, thus adversely affecting the water cycle.

Ans. Cellular respiration is the process by which organisms take up oxygen in order to breathe and digest food. Water is utilized for breaking large molecules that release energy in the form of ATP , while in a subsequent step the water molecules are released back into the cell, which in turn returns to the atmosphere, thus affecting the water cycle.

Ans. Rivers contain more water than streams and thus contribute more to the formation of water vapor through evaporation compared to a stream.

• Water Cycle – Britannica.com
• The Water Cycle – Khanacademy.org
• Water Cycle – Noaa.gov
• What Is The Hydrologic Cycle? – Worldatlas.com
• What is the Water Cycle? – Earth.com
• The Water Cycle – Coastgis.marsci.uga.edu

Article was last reviewed on Wednesday, May 17, 2023

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One response to “Water Cycle”

The first part of the water cycle is of course evaporation and transportation, but I don’t want to focus on that, I want to focus on the 2nd step which is sublimation. Sublimation is when snow or hail, or sleet falls down on a mountain and it quickly turns into water vapor by passing the liquid phase.Now lets skip to the last phase which is RIPC

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Hydrologic Cycle

The water cycle describes how water is exchanged (cycled) through Earth's land, ocean, and atmosphere.

Earth Science, Meteorology, Geography, Physical Geography, Geology

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The  water cycle  describes how water is exchanged (cycled) through Earth's land, ocean, and atmosphere. Water always exists in all three phases, and in many forms—as  lakes and  rivers ,  glaciers and  ice sheets , oceans and seas, underground  aquifers , and  vapor  in the air and clouds .

Evaporation , Condensation , and Precipitation

The water cycle consists of three major processes: evaporation, condensation, and precipitation.

Evaporation

Evaporation is the process of a liquid's surface changing to a gas. In the water cycle, liquid water (in the ocean, lakes, or rivers) evaporates and becomes water vapor.

Water vapor surrounds us, as an important part of the air we breathe. Water vapor is also an important  greenhouse gas . Greenhouse gases such as water vapor and carbon dioxide  insulate Earth and keep the planet warm enough to maintain life as we know it. Increasing amounts of greenhouse gases in the atmosphere also contribute to global warming.

The water cycle 's e vaporation process is driven by the sun. As the sun interacts with liquid water on the surface of the ocean, the water becomes an invisible gas (water vapor ). E vaporation is also influenced by  wind ,  temperature , and the  density  of the body of water.

Condensation

Condensation is the process of a gas changing to a liquid. In the water cycle, water vapor in the atmosphere condenses and becomes liquid.

Condensation can happen high in the atmosphere or at ground level.  Clouds form as water vapor condenses, or becomes more concentrated (dense). Water vapor condenses around tiny particles called  cloud condensation nuclei (CCN) . CCN can be specks of dust, salt, or  pollutants . Clouds at ground level are called  fog  or mist.

Like e vaporation , condensation is also influenced by the sun. As water vapor cools, it reaches its saturation limit, or  dew point .  Air pressure  is also an important influence on the dew point of an area.

Precipitation

As is the case with evaporation and condensation, precipitation is a process. Precipitation describes any liquid or solid water that falls to Earth as a result of condensation in the atmosphere. Precipitation includes rain, snow, and hail.

Fog is not precipitation. The water in fog does not condense sufficiently to precipitate, or liquefy and fall to Earth. Fog and mist are a part of the water cycle called suspensions: They are liquid water suspended in the atmosphere.

Precipitation is one of many ways water is cycled from the atmosphere to the earth or ocean.

Other Processes

Evaporation, condensation, and precipitation are important parts of the water cycle. However, they are not the only ones.

Runoff , for instance, describes a variety of ways liquid water moves across land.  Snowmelt , for example, is an important type of runoff produced as snow or glaciers melt and form streams or pools.

Transpiration  is another important part of the water cycle . Transpiration is the process of water vapor being released from plants and soil. Plants release water vapor through  microscopic   pores called  stomata . The opening of stomata is strongly influenced by light, and so is often associated with the sun and the process of e vaporation .  Evapotranspiration  is the combined components of e vaporation and transpiration , and is sometimes used to evaluate the movement of water in the atmosphere.

States of Water

Through the water cycle, water continually circulates through three states: solid, liquid, and vapor.

Ice is solid water. Most of Earth's fresh water is ice, locked in massive glaciers, ice sheets, and ice caps .

As ice melts, it turns to liquid. The ocean, lakes, rivers, and underground aquifers all hold liquid water.

Water vapor is an invisible gas. Water vapor is not evenly distributed across the atmosphere. Above the ocean, water vapor is much more abundant, making up as much as four percent of the air. Above isolated deserts, it can be less than one percent.

The Water Cycle and Climate

The water cycle has a dramatic influence on Earth's climate and  ecosystems .

Climate is all the  weather  conditions of an area, evaluated over a period of time. Two weather conditions that contribute to climate include humidity and temperature . These weather conditions are influenced by the water cycle .

Humidity is simply the amount of water vapor in the air. As water vapor is not evenly distributed by the water cycle, some regions experience higher humidity than others. This contributes to radically different climates. Islands or coastal regions, where water vapor makes up more of the atmosphere, are usually much more humid than inland regions, where water vapor is scarcer.

A region's temperature also relies on the water cycle . Through the water cycle , heat is exchanged and temperatures   fluctuate . As water e vaporates , for example, it absorbs energy and cools the local environment. As water condenses, it releases energy and warms the local environment.

The Water Cycle and the Landscape

The water cycle also influences the  physical geography  of Earth. Glacial melt and  erosion  caused by water are two of the ways the water cycle helps create Earth's physical features.

As glaciers slowly expand across a landscape , they can carve away entire  valleys , create mountain peaks, and leave behind rubble as big as boulders. Yosemite Valley , part of Yosemite National Park in the U.S. state of California, is a  glacial valley . The famous Matterhorn, a peak on the Alps between Switzerland and Italy, was carved as glaciers collided and squeezed up the earth between them. Canada's "Big Rock" is one of the world's largest " glacial erratics ," boulders left behind as a glacier advances or retreats.

Glacial melt can also create  landforms . The  Great Lakes , for example, are part of the landscape of the Midwest of the United States and Canada. The Great Lakes were created as an enormous ice sheet melted and retreated, leaving liquid pools.

The process of erosion and the movement of runoff also create varied landscapes across Earth's surface. Erosion is the process by which earth is worn away by liquid water, wind, or ice.

Erosion can include the movement of runoff. The flow of water can help carve enormous canyons, for example. These canyons can be carved by rivers on high plateaus (such as the Grand Canyon, on the Colorado Plateau in the U.S. state of Arizona). They can also be carved by  currents deep in the ocean (such as the Monterey Canyon, in the Pacific Ocean off the coast of the U.S. state of California).

Reservoirs and Residence Time

Reservoirs are simply where water exists at any point in the water cycle. An underground aquifer can store liquid water, for example. The ocean is a reservoir. Ice sheets are reservoirs. The atmosphere itself is a reservoir of water vapor.

Residence time  is the amount of time a water molecule spends in one reservoir. For instance, the residence time of "fossil water," ancient  groundwater  reservoirs, can be thousands of years.

Residence time for water in the Antarctic ice sheet is about 17,000 years. That means that a molecule of water will stay as ice for about that amount of time.

The residence time for water in the ocean is much shorter—about 3,200 years.

The residence time of water in the atmosphere is the shortest of all—about nine days.

Calculating residence time can be an important tool for developers and engineers. Engineers may consult a reservoir's residence time when evaluating how quickly a pollutant will spread through the reservoir, for instance. Residence time may also influence how communities use an aquifer.

Breaking the Cycle The water cycle can change. Glacial retreat is the process in which glaciers melt faster than their ice can be replaced by precipitation. Glacial retreat limits the amount of fresh water available on Earth. We are experiencing the fastest rate of glacial retreat in recorded history.

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The water cycle is often taught as a simple circular cycle of evaporation, condensation, and precipitation. Although this can be a useful model, the reality is much more complicated. The paths and influences of water through Earth’s ecosystems are extremely complex and not completely understood. NOAA is striving to expand understanding of the water cycle at global to local scales to improve our ability to forecast weather, climate, water resources, and ecosystem health.

The water cycle. (Image credit: Dennis Cain/NWS)

The water cycle on Earth

Water is essential to life on Earth. In its three phases (solid, liquid, and gas), water ties together the major parts of the Earth’s climate system — air, clouds, the ocean, lakes, vegetation, snowpack offsite link , and glaciers offsite link .

The water cycle shows the continuous movement of water within the Earth and atmosphere. It is a complex system that includes many different processes. Liquid water evaporates into water vapor, condenses to form clouds, and precipitates back to earth in the form of rain and snow. Water in different phases moves through the atmosphere (transportation). Liquid water flows across land (runoff), into the ground (infiltration and percolation), and through the ground (groundwater). Groundwater moves into plants (plant uptake) and evaporates from plants into the atmosphere (transpiration). Solid ice and snow can turn directly into gas (sublimation). The opposite can also take place when water vapor becomes solid (deposition).

See how NOAA science is safeguarding lives, economies, and a healthy water supply.

Water, society, and ecology

Water influences the intensity of climate variability and change. It is the key part of extreme events such as drought and floods . Its abundance and timely delivery are critical for meeting the needs of society and ecosystems.

Humans use water for drinking, industrial applications, irrigating agriculture, hydropower, waste disposal, and recreation. It is important that water sources are protected both for human uses and ecosystem health. In many areas, water supplies are being depleted because of population growth, pollution, and development. These stresses have been made worse by climate variations and changes that affect the hydrologic cycle.

A series of atmospheric rivers starting in late December 2022 through mid-January 2023 dropped feet of rain and snow across California and other parts of the West Coast.

Water and climate change

Climate change is affecting where, when, and how much water is available. Extreme weather events such as droughts and heavy precipitation , which are expected to increase as climate changes, can impact water resources. A lack of adequate water supplies, flooding, or degraded water quality impacts civilization — now and throughout history. These challenges can affect the economy, energy production and use, human health, transportation, agriculture, national security, natural ecosystems , and recreation.

An airborne mission finds a global belt of particle formation is making clouds brighter.

EDUCATION CONNECTION

The water cycle impacts ecosystems, economies, and our daily lives. The resources in this collection help teachers guide their students beyond the classic water cycle diagram and through the complex social and environmental issues that surround water. The water cycle provides the opportunity to explore the nature of science using models and empirical evidence. 

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Water Cycle

Introduction: (initial observation).

Rain and snow are the main sources of fresh water for people living on the earth. Both rain and snow come from the clouds; but, where do the clouds come from? It often seems that clouds appear from nowhere. One minute the sky is clear and then a few minutes later clouds form. Sometimes clouds come from far places. Wind moves the clouds from one area to the other.

If you live near a lake, ocean or forest, you may have seen water vapors rising from wet surfaces and disappearing in the air. Is it possible that the same vapors become visible again when they get to higher elevations? If the clouds come from oceans, forests and other surface waters then why doesn’t the rain water contain salt and other pollutants that exist in rivers and surface waters?

Is it possible that only pure water evaporates and all impurities stay behind?

In this project you will study, observe and demonstrate the water cycle.

This project guide contains information that you need in order to start your project. If you have any questions or need more support about this project, click on the “Ask Question” button on the top of this page to send me a message.

If you are new in doing science project, click on “How to Start” in the main page. There you will find helpful links that describe different types of science projects, scientific method, variables, hypothesis, graph, abstract and all other general basics that you need to know.

Project advisor

Adult supervision and support is required for the experiments of this project.

Information Gathering:

Find out what happens to the water that evaporates. Read books, magazines or ask professionals who might know in order to learn about water evaporation, clouds and precipitation. Keep track of where you got your information from.

Following are samples of information that you may find:

The Water Cycle

Background Information:

Earth was formed 4.6 billion years ago, but water was not present from the very beginning. At some point, possibly because of the heating of hydrogen and oxygen as Earth developed, water vapor began to form in the atmosphere. About 3.8 billion years ago, oceans formed and the cycle began. The same water that you drink today has been around since the oceans formed. Water is an important part of life on this planet. The water cycle is a complex process that gives us water to drink and provides us with climates that allow us to have food to eat. The earth has a limited amount of water, which keeps going around and around. It is a very important cycle in that it allows for life and helps sustain life on earth. Seventy percent of the earth’s surface is covered by water. Yet only 1% of that water is in the form to be used by humans and land animals. Water constantly changes from solid to liquid to gas. This cycle is what we call the water cycle.

Evaporation, condensation, and precipitation are the cycles of the water cycle.

Evaporation occurs when the sun heats up water in our oceans, lakes, and rivers and turns it into vapor or stream. This water vapor leaves the oceans, lakes, and rivers and moves up into the air. The water vapor settles in the troposphere where it condenses.

Condensation happens when warm and cold air meets in the troposphere. The water vapors in the air get cold and excess water condenses into either liquid water or ice, which then form clouds. If enough of this water forms into clouds, rain will begin if the weather is warm. If it is cold, it will snow. This process is called precipitation.

Precipitation is when so much water has condensed that the air cannot hold it any longer. The clouds get heavy and water falls back to the earth in the form of rain, hail, sleet or snow.

Essentially water in liquid form turns into a gas, then into a solid, and finally back into a liquid in a never-ending process.

Suggested References:

Do some research on water cycles, and draw a diagram to help you further understand this important cycle of the earth. Once you understand the water cycle and have done some research on it, you can observe the cycle in your own home. The links below should be very helpful in this preparation process. They should be used as a complement to your own research.

If you live in the United States, there are 40 trillion gallons of water above your head on an average day. Each day, about four trillion gallons of this water fall to Earth as precipitation, such as rain, snow, or hail. Some of the water that falls to Earth soaks into the ground and provides runoff to rivers, lakes, and oceans. The remainder—more than 2.5 trillion gallons—returns to the atmosphere through evaporation, and the process begins again.

This continuous process of precipitation and evaporation is called the water cycle, or hydrologic cycle.

Source…

Evaporation:

Evaporation is when the sun heats up water in rivers or lakes or the ocean and turns it into vapor or steam. The water vapor or steam leaves the river, lake or ocean and goes into the air.

Sample Experiment to show condensation

In this experiment we will go through all the water cycles and recreate them at home to further understand how they affect the whole world.

You can observe condensation very simply with a few items from around your house. Pour cold water into a glass and put it out on a hot day. You will see water form on the outside of the glass after a few minutes. Water vapor in the warm air turns back into liquid when it touches the cold glass.

You can also view evaporation very easily in your home. Have a parent assist you with putting some water in a kettle, and letting it come to a boil. As the water in the kettle becomes heated, you can watch the steam rise out of the kettle. The water is evaporating into the air.

You can then take a ceramic plate and put it in your freezer for an hour. Then take the plate out of the freezer and hold it about 1 ft. over the steam rising out of the kettle. Be careful that the steam does not burn your hands. You will see water droplets form on the plate. This is then called condensation. If a lot of water condenses on plate, it will start dripping down and this in turn is called precipitation!

Conclusions:

In this same way that you viewed the water cycle in your home, the water cycle occurs on our earth. What is the importance of what you have just done? Summarize what you just observed in your experiments. Describe exactly what happened and try to think of the implications of these procedures.

Question/ Purpose:

What do you want to find out? Write a statement that describes what you want to do. Use your observations and questions to write the statement.

The purpose of this project is to display water cycle. Show how the light and heat energy from the sun evaporate water and distributes water around the earth.

Identify Variables:

When you think you know what variables may be involved, think about ways to change one at a time. If you change more than one at a time, you will not know what variable is causing your observation. Sometimes variables are linked and work together to cause something. At first, try to choose variables that you think act independently of each other.

As a display project, you will not need to identify variables. In higher grades you may want to study the effect of one specific factor on the rate of evaporation or condensation. That is when you need to define variables.

For example you may want to study the effect of temperature on evaporation of water. In this case temperature will be the manipulated variable. The rate of evaporation is the responding variable.

Another example is when you want to determine the evaporation rate in different days. (Experiment 3) . In this case the independent variable is the day. The dependent variable is the amount of water evaporation from one square foot surface water.

Hypothesis:

Based on your gathered information, make an educated guess about what types of things affect the system you are working with. Identifying variables is necessary before you can make a hypothesis.

In a display project, you will not need to identify variables.

Experiment Design:

Design an experiment to test each hypothesis. Make a step-by-step list of what you will do to answer each question. This list is called an experimental procedure. For an experiment to give answers you can trust, it must have a “control.” A control is an additional experimental trial or run. It is a separate experiment, done exactly like the others. The only difference is that no experimental variables are changed. A control is a neutral “reference point” for comparison that allows you to see what changing a variable does by comparing it to not changing anything. Dependable controls are sometimes very hard to develop. They can be the hardest part of a project. Without a control you cannot be sure that changing the variable causes your observations. A series of experiments that includes a control is called a “controlled experiment.”

Experiment 1: What evaporates?

Introduction : Rain and snow do not contain salt and other pollutants usually found in the sea or other surface waters. In this experiment you will test to see if such material may evaporate along with water.

Procedure :

• Make some salty-polluted water by dissolving some salt and some water color in a cup of water.
• Transfer your polluted water to a plate and leave it outside under the sun for water to evaporate.
• After a few days, see weather the salts and water color evaporated or if they remained on the plate.
• Based on the result, write your conclusion.

Experiment 2: Water Displacement?

Introduction : Evaporation, condensation and precipitation are parts of a process that transfer large amounts of water from oceans to dry lands all over the globe on a daily bases.

This process is called water cycle. Without this process rivers, forests and lakes could not exist. In this experiment we will examine the process of water cycle and see how water is transferred from one area to the other.

• Get a two compartment plastic container with a lid that seals perfectly. Make sure that the divider is shorter than the sides of the container; in this way air can freely flow between the two compartments.
• Place the container on a flat surface in a sunny place in your backyard and then place a piece of stone or a block of wood under one side of the container. In this way the container will be slanted to one side.
• Fill the elevated compartment in half with water. Carefully place the lid on and cover the lower compartment with an aluminum foil to keep it cool.
• After 7 days carefully open the container. What do you see in the lower compartment. Can water evaporate from one compartment and condense and precipitate in the other compartment?

Variations:

The above experiment can also be performed in a glass or plastic aquarium.

A slanted glass on top allows the condensations to go towards elevations that you may make using real soil or a block of Styrofoam.

Use plastic plants or dry plants on the elevations to simulate vegetations.

What if we have no sunlight?

A 100 watt flood lamp mounted about 1 foot above the water area can work like sunlight. You may use a timer or manually turn off an on the light every hour to create day and night conditions for your model.

Experiment 3: Rate of water cycle

Introduction : The water cycle starts by evaporation of surface waters and perspiration by plants, and it ends when the water comes back down to the earth in the form of rain or snow. In this experiment you measure and record the amount of water evaporating from surface waters in different days.

Who must do this experiment?

If you are required to have a data table and possibly a graph for your project, you may try this experiment. In most cases 8th grade students are expected to present a data table and a graph with their project report or project display.

Measure 250 milliliters of water in a graduated cylinder and then transfer the water to a flat, square cooking tray. Try to use a tray that has an area of one square foot. If you don’t have a tray that measure one square foot, you can make one using an aluminum foil placed over a cardboard.

Place the tray outside in an open space, away from animals and birds.

After 24 hours transfer the water back to the measuring cylinder and observe the difference. Record how much water was evaporated.

Repeat this experiment in 5 different days and record the amount of evaporated water per square foot. Also record the outdoor weather temperature on those days.

Your results table may look like this:

Calculate and write the average daily evaporation in the last row of your data table.

Make a graph:

You can use a bar graph to visually present your results. Make one vertical bar for each day you repeat your experiment. The height of bar will show the amount of daily evaporation on that day.

If for some reason such as rain or animals your results become invalid, you will have to ignore the results of such days. If you have time, you may repeat your test a few more days to have at least 5 days of reliable results.

Materials and Equipment:

Material used in the above experiments are:

• Water Color
• Clear plastic container with 2 compartment
• Plastic aquarium
• Light bulb (100 watt) to simulate sunlight

Results of Experiment (Observation):

Experiments are often done in series. A series of experiments can be done by changing one variable a different amount each time. A series of experiments is made up of separate experimental “runs.” During each run you make a measurement of how much the variable affected the system under study. For each run, a different amount of change in the variable is used. This produces a different amount of response in the system. You measure this response, or record data, in a table for this purpose. This is considered “raw data” since it has not been processed or interpreted yet. When raw data gets processed mathematically, for example, it becomes results.

Calculations:

No calculations are required for this project.

Summary of Results:

Summarize what happened. This can be in the form of a table of processed numerical data, or graphs. It could also be a written statement of what occurred during experiments.

It is from calculations using recorded data that tables and graphs are made. Studying tables and graphs, we can see trends that tell us how different variables cause our observations. Based on these trends, we can draw conclusions about the system under study. These conclusions help us confirm or deny our original hypothesis. Often, mathematical equations can be made from graphs. These equations allow us to predict how a change will affect the system without the need to do additional experiments. Advanced levels of experimental science rely heavily on graphical and mathematical analysis of data. At this level, science becomes even more interesting and powerful.

Conclusion:

Using the trends in your experimental data and your experimental observations, try to answer your original questions. Is your hypothesis correct? Now is the time to pull together what happened, and assess the experiments you did.

Related Questions & Answers:

What you have learned may allow you to answer other questions. Many questions are related. Several new questions may have occurred to you while doing experiments. You may now be able to understand or verify things that you discovered when gathering information for the project. Questions lead to more questions, which lead to additional hypothesis that need to be tested.

Possible Errors:

If you did not observe anything different than what happened with your control, the variable you changed may not affect the system you are investigating. If you did not observe a consistent, reproducible trend in your series of experimental runs there may be experimental errors affecting your results. The first thing to check is how you are making your measurements. Is the measurement method questionable or unreliable? Maybe you are reading a scale incorrectly, or maybe the measuring instrument is working erratically.

If you determine that experimental errors are influencing your results, carefully rethink the design of your experiments. Review each step of the procedure to find sources of potential errors. If possible, have a scientist review the procedure with you. Sometimes the designer of an experiment can miss the obvious.

References:

List of web references

Water Vapor

Q. Since this project doesn’t have results or data, then how would I set up the project board. Is there an Abstract, conclusion or a purpose?

A. In a display project you do the experiments and write down your observations as the experiment results. Project board will have drawings, pictures and writings similar to what you have in your project guide. In addition to that you also write your observations and what you have learned from your experiments. If you need to have a data table, you can repeat the experiment 2 in 5 different days and record the amount of water displacement every day. Then convert the values to the ratio of total water in the container.

It is always important for students, parents and teachers to know a good source for science related equipment and supplies they need for their science activities. Please note that many online stores for science supplies are managed by MiniScience.

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• Published: 21 June 2023

How climate change alters the water cycle

Nature Water volume  1 ,  page 485 ( 2023 ) Cite this article

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Climate change is not just about getting drier or getting wetter when it comes to water availability. We should work towards a more comprehensive process understanding of the water cycle that accounts for human actions.

We cannot emphasize enough the importance of the water cycle. Explaining and predicting the changes in water availability is no easy task, as water is stored and moves naturally across its pools, namely the atmosphere, Earth’s surface and underground ( The Water Cycle ; USGS, 2022 ).

In the past two decades, climate science researchers have debated over two hypothesized frameworks for trends in water availability under climate change: that wet will get wetter and dry will become drier (WWDD) or that global aridification (GA) will happen. There exist extensive and sometimes contentious studies to evidence each hypothesis, leaving us wondering which one is correct.

There might be no definite right or wrong in this case. In their Review in this issue, Benjamin Zaitchik and colleagues examine the physical bases and limitations basis of WWDD and GA based on the water-cycle budgets, including precipitation, evapotranspiration, the sum of runoff and the change in water storage.

The validity and predictive capacity of each framework depend on the specific context. WWDD may hold if the change in atmospheric moisture flux divergence is equal to the change in precipitation minus evaporation. Zaitchik et al. reviewed the successes and failures of the WWDD and concluded that WWDD applies best if the so-called wet and dry areas are defined based on seasonality rather than long-term average conditions. It would fail for applications in predicting water availability over a specific land location.

The limitations of GA were discussed by firstly distinguishing meteorological, hydrological and agroecological aridity. The trends in each form of aridity are sensitive to the associated processes. GA may be valid for meteorological aridification considering only atmospheric supply (precipitation) and demand (for example, potential evapotranspiration, relative humidity or vapour pressure deficit), and for hydrological aridification when defined in terms of soil moisture, but seems not to hold for runoff (hydrological aridification) or for agroecological aridification that considers ecological change. Like the WWDD, GA should also not be mistaken for water availability predictions at precise locations.

Despite the limitations and complications of both frameworks, they can be useful for developing and testing hypotheses through careful considerations of appropriated contexts in both atmospheric and water perspectives, particularly the temporal and spatial scales. However, the widely used phrases WWDD and GA may have led to misapplication of the frameworks and misunderstanding of the responses of the water cycle to the changing climate. The phrases may be easy to remember and attract attention, but they do not refer to any specific process or variable that underlies the frameworks.

We might all hope for a definitive answer to the question of whether there will be more or less water for us in the future, but the reality is too complicated to be explained by a simple answer. The Review tells the story of us learning about the water cycle and seeking answers: from observations to hypotheses, then to applications and theories. As emphasized by Zaitchik et al., we would be better off using simplified frameworks as an entry point for studying processes, focusing on detangling processes in the water cycle rather than assuming generalized outcomes, and on a careful assessment of regional- and seasonal-scale changes. And, of course, we should also account for the interference of human actions on the water cycle.

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How climate change alters the water cycle. Nat Water 1 , 485 (2023). https://doi.org/10.1038/s44221-023-00104-6

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How does the water cycle work?

Water molecules are heated by the sun and turn into water vapor that rises into the air through a process called evaporation. Next, the water vapor cools and forms clouds, through condensation. Over time, the clouds become heavy because those cooled water particles have turned into water droplets. When the clouds become extremely heavy with water droplets, the water falls back to earth through precipitation (rain, snow, sleet, hail, etc). The process continues in a cyclical manner.

Learn more about Earth's water cycle on the Precipitation Education website.

Freshwater seems abundant, but when accounting for all the water on Earth, it's in limited supply. Just three percent of the water on our planet is freshwater. A majority of this water, about two percent of the world total, is contained in glaciers and ice sheets or stored below ground. The remaining one percent is found in lakes, rivers and wetland areas or transported through the atmosphere in the form of water vapor, clouds and precipitation. Rain and snowfall replenish freshwater sources, making it vital to know when, where and how much water is falling at any given time. Using NASA's Global Precipitation Measurement satellite, researchers can track precipitation worldwide and monitor levels from space. For more information, visit http://water.usgs.gov/edu/earthwherew ... This video is public domain and can be downloaded at: http://svs.gsfc.nasa.gov/goto?11619

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• Biology Article

Water Cycle

What is the Water Cycle? Water Cycle Diagram Stages of Water Cycle Implications of Water Cycle Frequently Asked Questions

What is the Water Cycle?

Water Cycle Diagram

During this process, water changes its state from one phase to another, but the total number of water particles remains the same. In other words, if it were possible to collect and boil 100 gms of water, it will still retain a mass of 100 gms as steam. Likewise, if 100 gms of steam is collected and condensed, the resultant water would still weight 100 gms.

Water changes its state through a variety of processes from evaporation, melting and freezing, to sublimation, condensation, and deposition. All these changes require the application of energy.

Stages of Water Cycle

There are many processes involved in the movement of water apart from the major steps given in the above water cycle diagram. Listed below are different stages of the water cycle.

1. Evaporation

The sun is the ultimate source of energy, and it powers most of the evaporation that occurs on earth. Evaporation generally happens when water molecules at the surface of water bodies become excited and rise into the air. These molecules with the highest kinetic energy accumulate into water vapour clouds. Evaporation usually takes place below the boiling point of water. Another process called evapotranspiration occurs when evaporation occurs through the leaves of plants. This process contributes to a large percentage of water in the atmosphere.

2. Sublimation

Sublimation occurs when snow or ice changes directly into water vapour without becoming water. It usually occurs as a result of dry winds and low humidity. Sublimation can be observed on mountain peaks, where the air pressure is quite low. The low air pressure helps to sublimate the snow into water vapour as less energy is utilised in the process. Another example of sublimation is the phase where fog bellows from dry ice. On earth, the primary source of sublimation is from the ice sheets covering the poles of the earth.

3. Condensation

The water vapour that accumulated in the atmosphere eventually cools down due to the low temperatures found at high altitudes. These vapours become tiny droplets of water and ice, eventually coming together to form clouds.

4. Precipitation

Above 0 degrees centigrade, the vapours will condense into water droplets. However, it cannot condense without dust or other impurities. Hence, water vapours attach itself on to the particle’s surface. When enough droplets merge, it falls out of the clouds and on to the ground below. This process is called precipitation (or rainfall). In particularly cold weather or extremely low air pressure, the water droplets freeze and fall as snow or hail.

5. Infiltration

Rainwater gets absorbed into the ground through the process of infiltration. The level of absorption varies based on the material the water has seeped into. For instance, rocks will retain comparatively less water than soil. Groundwater can either follows streams or rivers. But sometimes, it might just sink deeper, forming aquifers.

If the water from rainfall does not form aquifers, it follows gravity, often flowing down the sides of mountains and hills; eventually forming rivers. This process is called runoff. In colder regions, icecaps form when the amount of snowfall is faster than the rate of evaporation or sublimation. The biggest icecaps on earth are found at the poles.

All the steps mentioned above occur cyclically with neither a fixed beginning nor an end.

Also Read:  Back to the Oceans

Implications of Water Cycle

• The water cycle has a tremendous impact on the climate. For instance, the greenhouse effect will cause a rise in temperature. Without the evaporative cooling effect of the water cycle, the temperature on earth would rise drastically.
• The water cycle is also an integral part of other biogeochemical cycles.
• Water cycle affects all life processes on earth.
• The water cycle is also known the clean the air. For instance, during the process of precipitation, water vapours have to attach themselves on to particles of dust. In polluted cities, the raindrops, apart from picking up dust, also pick up water-soluble gas and pollutants as they fall from the clouds. Raindrops are also known to pick up biological agents such as bacteria and industrial soot particles and smoke.

Read more about the water cycle with diagram by registering @  BYJU’S Biology

• Biogeochemical cycles
• Oxygen Cycle
• Carbon Cycle
• Nitrogen Cycle

Frequently Asked Questions

What are the major 4 steps in the water cycle.

The major 4 steps are evaporation of water, then condensation, precipitation and collection. The sun evaporates water sources and contributes to the formation of water vapor. These water vapour accumulate in the atmosphere as clouds. The vapours condense into water droplets and when enough droplets merge, it falls out of the clouds as rain.

What is the difference between evaporation and condensation?

Evaporation is a process by which water changes into water vapour. Condensation is an opposite process by which water vapour is converted into tiny droplets of water.

Why is water cycle important?

Water cycle has a huge impact on determining the global climate. It is also an integral part of other biogeochemical cycles. It affects all life processes on Earth either directly or indirectly.

Put your understanding of this concept to test by answering a few MCQs. Click ‘Start Quiz’ to begin!

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Precipitation and the Water Cycle

Precipitation is water released from clouds in the form of rain, freezing rain, sleet, snow, or hail. Precipitation is the main way atmospheric water returns to the surface of the Earth. Most precipitation falls as rain.

•   Water Science School HOME   •  Water Basics topics   •  The Water Cycle   •

Water cycle components   »   Atmosphere   ·   Condensation   ·   Evaporation   ·   Evapotranspiration   ·   Freshwater lakes and rivers    ·   Groundwater flow   ·   Groundwater storage   ·   Ice and snow   ·   Infiltration   ·   Oceans   ·   Precipitation   ·   Snowmelt   ·   Springs   ·   Streamflow   ·   Sublimation   ·   Surface runoff

Clouds  floating overhead contain water vapor and cloud droplets, which are small drops of condensed water. These droplets are way too small to fall as precipitation, but they are large enough to form visible clouds. Water is continually  evaporating and condensing   in the sky. If you look closely at a cloud, you can see some parts disappearing (evaporating) while other parts are growing (condensing). Most of the condensed water in clouds does not fall as precipitation because their fall speed is not large enough to overcome updrafts which support the clouds. 

For precipitation to happen, first tiny water droplets must condense on even tinier dust, salt, or smoke particles, which act as a nucleus, binding them together. Water droplets may grow as a result of additional condensation of water vapor when the particles collide. If enough collisions occur to produce a droplet with a fall velocity which exceeds the cloud updraft speed, then it will fall out of the cloud as precipitation. This is not a trivial task since millions of cloud droplets are required to produce a single raindrop.  

A more efficient mechanism for producing a precipitation-sized drop, is a process which leads to the rapid growth of ice crystals at the expense of the water vapor present in a cloud. These crystals may fall as snow, or melt then fall as rain. This process is known as the Bergeron-Findeisen process.

How much water falls during a storm? 

You might be surprised at the number of gallons of water that fall from the sky in even a small but intense storm. One inch of rain falling on just a single acre results in 27,154 gallons of water on the landscape. If you'd like to know how much water falls during a storm, use our Interactive Rainfall Calculator ( English units  or  Metric units ) . Just enter an area size and rainfall amount and see how many gallons of water reach the ground.   

What do raindrops look like?

Small raindrops, those with a radius of less than 1 millimeter (mm), are spherical, like a round ball. As droplets collide and grow in size, the bottom of the drop begins to be affected by the resistance of the air it is falling through. The bottom of the drop starts to flatten out until at about 2-3 mm in diameter the bottom is quite flat with an indention in the middle - much like a hamburger bun. Raindrops don't stop growing at 3 millimeters, though, and when they reach about 4-5 mm, things really fall apart. At this size, the indentation in the bottom greatly expands forming something like a parachute. The parachute doesn't last long, though, and the large drop breaks up into smaller drops.   

Precipitation rates vary geographically and over time

In 2017, Colombia received the greatest amount of precipitation at 3,240 mm for the year. Contrast that with Egypt for the same year, during which they received only 18 mm of precipitation for the year. Explore more annual precipitation data on this interactive site from Our World in Data or at  Precipitation Climatology | NASA Global Precipitation Measurement Mission .  

Precipitation size and speed

Have you ever watched a raindrop hit the ground during a large rainstorm and wondered how big the drop is and how fast it is falling? Or maybe you've wondered how small fog particles are and how they manage to float in the air. The table below shows the size, velocity of fall, and the density of particles (number of drops per square foot/square meter of air) for various types of precipitation, from fog to a cloudburst. 

Source: Lull, H.W., 1959, Soil Compaction on Forest and Range Lands, U.S. Dept. of Agriculture, Forestry Service, Misc. Publication No.768

Sources and more information

• Rain: A Water Resource , USGS General Interest Publication

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The Water Cycle

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NOAA Water Cycle Resources

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You may think every drop of rain falling from the sky, or each glass of water you drink, is brand new, but it has always been here, and is a part of the water cycle.  At its most basic, the water cycle is how water continuously moves from the ground to the atmosphere and back again.  As it moves through this cycle, it changes forms.  Water is the only substance that naturally exists in three states on Earth – solid, liquid, and gas.

Over 96% of total global water is in the ocean, so let’s start there.  Energy from the sun causes water on the surface to evaporate into water vapor – a gas.  This invisible vapor rises into the atmosphere, where the air is colder, and condenses into clouds.  Air currents move these clouds all around the earth.

Water drops form in clouds, and the drops then return to the ocean or land as precipitation - let’s say this time, it’s snow.  The snow will fall to the ground, and eventually melts back into a liquid and runs off into a lake or river, which flows back into the ocean, where it starts the process again.

That’s just one path water can take through the water cycle.  Instead of snow melting and running off into a river, it can become part of a glacier and stay there for a long, long time.  Or rain can seep into the ground and become groundwater, where it’s taken up by plants.  It can then transpirate to gas directly through the leaves and return to the atmosphere.  Or, instead of being taken up by the plant, the groundwater can work its way up to a lake, river, spring, or even the ocean.

As you can see, the water cycle can be a very complicated process.  And all its paths through Earth’s ecosystems are complex and not completely understood.

Transcripción

• Open access
• Published: 20 March 2018

Forests, atmospheric water and an uncertain future: the new biology of the global water cycle

• Douglas Sheil   ORCID: orcid.org/0000-0002-1166-6591 1  

Forest Ecosystems volume  5 , Article number:  19 ( 2018 ) Cite this article

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Theory and evidence indicate that trees and other vegetation influence the atmospheric water-cycle in various ways. These influences are more important, more complex, and more poorly characterised than is widely realised. While there is little doubt that changes in tree cover will impact the water-cycle, the wider consequences remain difficult to predict as the underlying relationships and processes remain poorly characterised. Nonetheless, as forests are vulnerable to human activities, these linked aspects of the water-cycle are also at risk and the potential consequences of large scale forest loss are severe. Here, for non-specialist readers, I review our knowledge of the links between vegetation-cover and climate with a focus on forests and rain (precipitation). I highlight advances, uncertainties and research opportunities. There are significant shortcomings in our understanding of the atmospheric hydrological cycle and of its representation in climate models. A better understanding of the role of vegetation and tree-cover will reduce some of these shortcomings. I outline and illustrate various research themes where these advances may be found. These themes include the biology of evaporation, aerosols and atmospheric motion, as well as the processes that determine monsoons and diurnal precipitation cycles. A novel theory—the ‘biotic pump’—suggests that evaporation and condensation can exert a major influence over atmospheric dynamics. This theory explains how high rainfall can be maintained within those continental land-masses that are sufficiently forested. Feedbacks within many of these processes can result in non-linear behaviours and the potential for dramatic changes as a result of forest loss (or gain): for example, switching from a wet to a dry local climate (or visa-versa). Much remains unknown and multiple research disciplines are needed to address this: forest scientists and other biologists have a major role to play. New ideas, methods and data offer opportunities to improve understanding. Expect surprises.

Introduction and background

The availability of water determines where life, including people, can occur and is in turn influenced by such life—again including people. Increasing human populations and improving living standards are impacting the earth’s surface (Godfray et al. 2010 ; Sayer et al. 2013 ). Over one third of the Earth’s ice-free land comprises agriculture, pasture and urbanisation (Ramankutty et al. 2008 ). One and a half million square kilometres of dense tree-cover were lost between 2000 and 2012 (gross 2.3 million lost and 0.8 million gained, Hansen et al. 2013 ). At the same time, evaluations indicate major increases in people with impeded access to fresh water and also in those exposed to floods (e.g., Arnell et al. 2016 ). For those confronting these issues, a concern is whether we know enough to understand, predict, and address how land cover influences water availability.

Water vapour comprises one quarter of 1 % of the mass of the atmosphere—equivalent to just two and half centimetres of liquid over the entire Earth (atmospheric water in the form of liquid droplets and ice adds less than one hundredth to this miniscule total). The behaviour of this atmospheric water nonetheless governs water availability on land. Terrestrial life, including human life, depends on and impacts this availability. Understanding these links and vulnerabilities is vital if we want to avoid the water scarcity, droughts and floods that may otherwise result from changing land cover.

Global vegetation and climate are linked in both directions: when climate changes, so will vegetation, and when vegetation changes, so will the climate. These links are more important, more complex, and more poorly characterised than most people realise.

Water availability raises more tangible concerns for most people than do temperature and carbon. In any case, those concerned with temperature recognise 1) that around half the solar energy that falls on land is converted into the evaporation of water thus cooling the land surface (Pokorny et al. 2010 ; Wang and Dickinson 2012 ), 2) that water vapour is the dominant greenhouse gas on our planet (Ravishankara 2012 ; Sherwood et al. 2010 ) and 3) that the distribution of clouds and snow cover exert a major influence on planetary albedo (the proportion of incident light reflected back into space) and energy balance (Donohoe and Battisti 2011 ; He et al. 2014 ). Those concerned with carbon recognise that water is the most limiting factor for terrestrial ecosystem carbon uptake, and that uncertainties over water imply uncertainties over biomass and carbon fixation (Polis 1999 ; Good et al. 2013 ; Bernacchi and VanLoocke 2015 ; Thorley et al. 2015 ; Viglizzo et al. 2016 ; Taylor et al. 2017 ; Zhu et al. 2017 ). Furthermore, those concerned with environmental conservation, stability and the maintenance of species diversity recognise both the significance of freshwater biodiversity (supporting over 126,000 species of plants and animals, many of them vulnerable, on 0.8% of the world’s surface, Garcia-Moreno et al. 2014 ) and the links between terrestrial diversity and moisture (Kreft and Jetz 2007 ; Sheil et al. 2016 ; Viglizzo et al. 2015 ).

In this article, I review our understanding of vegetation-climate relationships focusing on how land cover, particularly trees, influences the atmospheric water-cycle. I focus on challenges and advances rather than policy and synthesis (e.g., McAlpine et al. 2010 ; Mahmood et al. 2013 ; Lawrence and Vandecar 2015 ; Ellison et al. 2017 ) or specific regions (e.g., McAlpine et al. 2009 ; Nobre 2014 ). For reasons that will become apparent, I shall avoid the substantial literature focused on climate simulations and scenarios (Mahmood et al. 2013 ; Devaraju et al. 2015 ; Salazar et al. 2015 ; Mahmood et al. 2016 ; Prestele et al. 2016 ). I target forest scientists and others outside atmospheric sciences and thus minimise jargon. I first describe the global water-cycle, and then examine key aspects: evaporation, aerosols, winds and their interactions.

The water-cycle

Precipitation—rain, snow and hail in all their forms—denotes the stage in the water-cycle when water falls to earth from the atmosphere. Most of us rely on this water, and demand is growing. Between 1992 and 2015 the sum total of global freshwater resources divided by the total human population has declined by over 25% (from around 8000 m 3 to below 6000 m 3 per person) (Ripple et al. 2017 ). Availability is uneven and often limited. Two thirds of the global population already experience water scarcity for more than a month each year while half a billion face year-round scarcity (Mekonnen and Hoekstra 2016 ). Those who rely on the world’s finite ground water reserves are vulnerable to their accelerating depletion (Wada et al. 2010 ).

Reliability and variation in precipitation matter. Extreme events can be catastrophic: from 1900 to 2013 more than eleven million lost their lives as a result of drought and seven million people died as a result of floods, while half a billion required emergency aid due to such events (Sheil 2014 ).

While much atmospheric water vapour originates from the oceans much is also recycled off land. Of the approximately 117,600 km 3 of water that falls to the terrestrial surface as precipitation each year, less than a half 45,800 km 3 (39%) comes from the ocean while the majority (71,800 km 3 , or 61%), derives from the land (Schneider et al. 2017 ). (For a discussion of how such values are estimated, and the associated uncertainties, see, e.g., Gimeno et al. 2012 ). Thus, most terrestrial precipitation depends on moisture derived from land. More than half of this land-derived atmospheric moisture comes from transpiration by plants, though the precise fraction remains contested (Jasechko et al. 2013 ; Sutanto et al. 2014 ; Wei et al. 2017 ).

One recent study estimated that land cover changes have caused a 5 to 6% reduction in global atmospheric moisture (Sterling et al. 2013 ). Comparing this with growing demand for water and the finite supplies available, the authors concluded that impacts on the global water-cycle were already “much closer … than previously thought” to further negative impacts on human lives (Sterling et al. 2013 ).

The degree to which precipitation depends on moisture derived from land varies with location, ranging from low, for some oceanic islands, to high in some continental regions such as northwest China (van der Ent et al. 2010 ; Zhao et al. 2016 ). The Amazon Basin, East Africa, Western North America, and central Eurasia are major sources of water vapour for areas downwind (van der Ent et al. 2010 ). The typical distances that moisture evaporated from land travels in the atmosphere before it falls to earth once more are in the order of 500–5000 km meaning that large-scale influences in land cover are crucial (van der Ent and Savenije 2011 ). One recent study to evaluate these links concluded that even in several major river basins, including those of the Amazon, Congo and Yangtze, precipitation was more influenced by land-use change occurring outside the basin than inside (Wang-Erlandsson et al., 2017 ).

As total global precipitation and evaporation balance, any reduction in precipitation at one time or place may result in an increase at another and visa-versa (Rosenfeld et al. 2008 ). There are many examples where increasing frequencies and severities of droughts and floods appear to follow disruptions to the water-cycle (Millán 2014 ; Hirsch and Archfield 2015 ; Erfanian et al. 2017 ). While global precipitation held relatively constant over recent decades, observations indicate that increases occurred over the tropical oceans and higher latitudes (much of North America and Eurasia), while declines occurred over Africa and various mid latitudes (notably the Mediterranean and southern Asia) (Trenberth 2011 ; Adler et al. 2017 ). The Intergovernmental Panel on Climate Change (IPCC) expresses “medium confidence” that human activities influenced precipitation intensity (especially Northern Hemisphere) over the second half of the twentieth century (Stocker et al. 2013 ). The ability to understand, predict and address such changes is a crucial research goal.

Our best integrated-understanding of how the global water-cycle functions is arguably embodied in the simulation models used in climate sciences. The models used by climate scientists to simulate global climate and investigate how it changes—General Circulation Models, Global Climate Models, and Earth System Models (henceforth “models”)—have become increasingly sophisticated. Complexity has increased as additional phenomena and their associated sub-models are added and refined. Various aspects of vegetation cover, such as leaf area phenology, canopy roughness and rooting depth are generally included with varying levels of sophistication (Bonan 2008 ; Guimberteau et al. 2017 ).

Researchers recognise various problems with these models (Stevens and Bony 2013 ; Shepherd 2014 ; Marotzke et al. 2017 ). For example, one summary noted that `most models simulate precipitation that occurs prematurely and too often, and with insufficient intensity` (Trenberth 2011 ). Another review highlighted that the inability to model terrestrial precipitation represented the principle ‘roadblock to progress in climate science’ (Stevens and Bony 2013 ). Another more recent review written by modellers noted that ‘The global water-cycle — from the formation of clouds, to the release of precipitation, to land surface hydrology including its interaction with the atmosphere, to water storage and release in the cryosphere — remains one of the least understood natural cycles. Hence, the predictions of this cycle in a changing climate are amongst the most uncertain. This constitutes a major challenge in ascertaining future water availability’ (Marotzke et al. 2017 ).

Using models to make predictions assumes that they embody all the key relationships determining the changes under consideration in an adequate manner. Many parameters in these complex models are not derived from measurements, but from tuning within and among sub-models. Such tuning involves an iterative process of adjusting values to ensure that behaviours and outputs appear sufficiently similar to past periods (Hourdin et al. 2017 ; Loehle 2017 ). But not all aspects of such complex models can be perfected simultaneously. For example, tuning a model to better represent seasonal shifts in precipitation can result in less accurate mean values (Kim et al. 2012 ).

One way to test models is to see how their behaviours and predictions match reality (without local tuning). If they match we may be reassured, but if they don’t, we conclude that something is missing or incorrect. Such checks reveal discrepancies: for example, models indicate that rainfall over the major land masses of Indonesia is lower than that over the neighbouring oceans though the reverse is true (Qian 2008 ) and that the flow of water out of the Amazon River should be half what is observed (e.g., Hagemann et al. 2011 ).

There are other striking mismatches between models and observations. For example, data concerning long-term variation in precipitation within and among different regions of the globe are not captured by models (Ljungqvist et al. 2016 ). In addition, it has long been recognised that while observations indicate a decline in terrestrial evaporation as temperatures increase, models indicate the reverse (Roderick and Farquhar 2002 ; Roderick et al. 2009 ). Looking at the details we find that models predict that atmospheric water will increase by about 7% for each degree Kelvin of surface warming, with global precipitation increasing at a markedly slower rate varying from 1% to 3% per degree Kelvin (depending on the model) (Wentz et al. 2007 ). Observations, in contrast, find that global atmospheric water and precipitation are increasing at a similar rate (Wentz et al. 2007 ). Efforts to reconcile these observations are hampered by an inability to predict changes in wind speeds and circulation patterns (Jian et al. 2016 ). Models also make diverging predictions regarding circulation patterns (Yim et al. 2017 ). Shortcomings are also found in predicting the changing seasonal behaviour of monsoon climates as in India, where the winter winds blow from northeast and are relatively dry while the summer winds blow from the southwest and bring heavy rain (e.g., Acharya et al. 2011 ; Niu et al. 2015 ).

There are multiple aspects to this uncertainty about the dynamics of water in the climate system (Stevens and Bony 2013 ; Shepherd 2014 ; Hegerl et al. 2015 ). For example, the behaviour of clouds, and cloud related feedbacks, continue to vex climate researchers—with large differences among models and also between models and observations (Ceppi et al. 2017 ). Attention has also focused on resolution and the effects of terrain (Peatman et al. 2014 ; Li et al. 2017 ). The influence of ocean temperatures and climate cycles, such as El Niño-La Niña, and the processes that govern these relationships, have also been highlighted (Miralles et al. 2014 ). Discrepancies likely reflect multiple factors (Wang and Dickinson 2012 ; Mahmood et al. 2013 ; Heald and Spracklen 2015 ). Uncertainties related to land cover appear relatively unexplored. In any case, there is agreement that large discrepancies and gaps in models and in fundamental understanding persist.

Most studies of how land use change influences climate and hydrology rely on models (e.g., Piao et al. 2007 ; Unger 2014 ; Garcia et al. 2016 ; Mahowald et al. 2017 ). These models are imperfect (Hagemann et al. 2013 ; Maraun 2016 ). If they omit or misrepresent key processes or mechanisms, then their results, if unconfirmed by observations, should be treated with caution.

One consequence of these shortcomings in current models is that climate researchers have invited physical scientists to assist them (Bony et al. 2015 ; Schiermeier 2015 ). I believe that they should also call forest scientists and other biologists. Many model discrepancies likely result from poorly characterised biological processes. As the other uncertainties are addressed, an increasing fraction of the remaining unresolved details will reflect biology (Sheil 2014 ).

Atmospheric moisture can result from various sources and processes over land: evaporation from open water, soil, wet terrestrial surfaces, wet vegetation ‘interception’ and transpiration (i.e. from within vegetation, Savenije 2004 ). In the previous section, we noted how most terrestrial precipitation is recycled from the land surface and that more than half of this derives from transpiration by plants.

All higher plants control when and how much water vapour they release (McAdam and Brodribb 2012 ). Leaves and other plant parts are typically waxy and relatively impermeable, with most gas exchange and water loss occurring through stomatal pores. Stomata control the entry of carbon dioxide into the leaf and the emission of water through transpiration (simultaneously regulating leaf temperature, Matthews et al. 2017 ). These adjustable pores evolved around 400 million years ago and have influenced our planet’s water-cycle ever since (Berry et al. 2010 ; Brodribb and McAdam 2017 ). The control of these pores determines the exchange of gases, including water vapour and carbon dioxide, between the plants’ intercellular space and the external atmosphere. The behaviour of stomatal pores is assumed to optimize carbon gain (growth), depending on environmental conditions including access to water and the risks that arise from drought, but our understanding of these relationships remains a “work in progress” (Klein 2014 ; Martin-StPaul et al. 2017 ; Matthews et al. 2017 ; Meinzer et al. 2017 ). Furthermore, trees capture nutrients by drawing in soil water, thus increased transpiration rates can be a response to low nutrient environments (Matimati et al. 2013 ; Huang et al. 2017 ).

The dynamics of transpiration are surprisingly complex. For example, the stomata of tropical trees often close after a few hours of intense photosynthesis due to temporary depletion of available water, though this behaviour varies among species, and with conditions (Zhang et al. 2013 ). There are also processes that somehow coordinate stomatal opening and closing within and even among leaves (Kaiser and Paoletti 2014 ) and that can lead to pulsed, cyclic and even chaotic patterns of moisture release (Johnsson 2015 ). There is some evidence, from Costa Rica and Finland (in summer) that a cyclic pattern of moisture release occurs over actively transpiring forests with a mean period of 70 to 80 min (Bunyard 2014 and pers. comm. December 2017). Furthermore, evidence shows that most types of plants in every biome where it has been examined continue to lose water to some degree through their open stomata at night—the degree of this nocturnal transpiration varies among species, and the functional significance is not well understood, though it may (at least in some cases) relate to competition for nutrients (Dawson et al. 2007 ; Cramer et al. 2009 ; Rosado et al. 2012 ; Bucci et al. 2016 ). Night-time sap-flow and transpiration are greatest in species with rapid growth, high concentrations of leaf nitrogen and lower shade tolerances (Marks and Lechowicz 2007 ). Comprehensive modelling of all these processes and relationships remains a challenge (Buckley 2017 ; Franks et al. 2017 ; Matthews et al. 2017 ).

The water evaporated from wet surfaces, including that intercepted by and held on vegetation, is also a major source of atmospheric moisture. Indeed there are theoretical reasons to suggest that this moisture is more likely to be recycled locally than that from transpiration (van der Ent et al. 2014 ).

In any case, the sum emission of water vapour from forests (transpiration and evaporation from other sources combined) typically surpasses that from other vegetation and even from open water. Though there are uncertainties concerning the best means to estimate these values (see review and discussion in Fisher et al. 2009 ), tropical forest regions typically evaporate more than one meter of water each year, Footnote 1 averaging 1.37 m per year (m∙yr. − 1 , standard deviation 0.18 m∙yr. − 1 ) across the Amazon basin (Fisher et al. 2009 ) and 1.32 m∙yr. − 1 (standard deviation 0.08 m∙yr. − 1 ) across Borneo (Kume et al. 2011 ). Local values can be much higher, and some forests exceed 2.2 m∙yr. − 1 (Loescher et al. 2005 ). Such water is important. One pantropical evaluation examined rainfall across the tropics: for each location the researchers identified the path of the local wind over the previous 10 days and found that those that had traversed closed forest typically produced more than twice as much rain as those that had traversed open land (Spracklen et al. 2012 ).

Trees achieve high rates of transpiration by maintaining their high leaf area in moving air and by possessing roots able to access moisture even when the upper soil is dry. Furthermore, trees can use moisture stored in their stems when their needs exceed uptake—such stored water can provide 20%–30% of transpired water and this is typically replaced at night, though such transpiration may be maintained over several days, even with a growing moisture deficit (Čermák et al. 2007 ). In some locations trees capture, and then re-evaporate, significant moisture from clouds, fog or dew (Holder 2004 ; Fu et al. 2016 ; Wang et al. 2017 )—a process often boosted by epiphytic vegetation (Holscher et al. 2004 ; Villegas et al. 2008 ; Stanton et al. 2014 ). While water on leaf surfaces inhibits transpiration, the foliage of plants in wet environments tend to dry rapidly (Smith and McClean 1989 ; O'Brien et al. 2004 ). Other processes may play a role too, for example, condensation on cool stems (Lakatos et al. 2012 ; Wang et al. 2017 ), and redistribution of moisture in the soil profile due to the presence of roots, (Dawson 1996 ; Domec et al. 2010 ; Neumann and Cardon 2012 ; Prieto et al. 2012 ). The influence of air movements and turbulence (due to canopy structure and other features) on transpiration and water loss likely also plays a role (Hollinger et al. 1994 ; Vanclay 2009 ).

Forest soils tend to be deeper, more porous and more permeable than other soils, increasing moisture infiltration and storage and reducing runoff (Malmer et al. 2010 ). Increased runoff is sometimes seen as desirable. For example, hydrologists note that the higher water use associated with dense tree cover reduces water availability compared with low tree cover (Bruijnzeel 1990 ; Sahin and Hall 1996 ; Viglizzo et al. 2016 ). Thus, for example, one influential meta-analysis found that annual stream flow typically declined by over a third where closed-forests were planted, with larger losses at drier sites (all but three of the 506 assessments being Eucalyptus or Pinus , and all but two being outside the tropics) (Jackson et al. 2005 ). But there are important caveats, including that water gained by streams and rivers will no longer fall as rain downwind, that different effects operate at different scales (thus forest loss in one area may increase local runoff but may still reduce regional rain by a larger amount), and that comparing open land and dense forests neglects the non-linear relationships with infiltration and soil desiccation that may influence outcomes at intermediate tree densities (Ilstedt et al. 2007 ; Malmer et al. 2010 ; Thompson et al. 2010 ). Studies in African drylands demonstrate the importance of such caveats by showing that there are non-zero tree densities where the benefits of improved soil infiltration can greatly exceed evaporation losses and can substantially increase, rather than deplete, ground water when compared to treeless areas (Ilstedt et al. 2016 ).

Despite the increasing number of studies we know less about the influence of forest restoration or expansion on water than is generally acknowledged (Malmer et al. 2010 ). One recent review notes that while most studies continue to report reduced runoff, these results provide an incomplete picture as infiltration, rainfall, intermediate-stem-densities and scale-effects are generally neglected (Filoso et al. 2017 ). They also highlight that while local water yields often decline under young regrowth forests, yields change and may recover as the vegetation matures, though this trend is beyond most short-term studies (Filoso et al. 2017 ).

Observations indicate that changes in forest cover influence the local and regional climate. I will not attempt a synthesis here as these observations are reviewed elsewhere (e.g., Bruijnzeel 2004 ; Bonan 2008 ; Lawrence and Vandecar 2015 ). To summarise: reducing forest cover often correlates with some decline in rainfall and cloud cover, though specific cases may be idiosyncratic. In all such correlations causal relationships are hard to prove given the impossibility of a replicated study and the multiple potential influences.

Atmospheric aerosols

Under common atmospheric conditions water vapour neither freezes nor condenses without the presence of atmospheric particles or droplets—aerosols—hence these can exert a major influence on clouds and precipitation (Després et al. 2012 ). Any change in the abundance, character or dynamics of these aerosols will impact the water-cycle (Rosenfeld et al. 2008 ; Rosenfeld et al. 2014 ; Fan et al. 2016 ). The key relationships are non-linear. For example, increasing aerosol densities can increase or decrease both cloud cover and precipitation (Rosenfeld et al. 2008 ) and influence associated atmospheric behaviours (Koren et al. 2014 ; Seinfeld et al. 2016 ). Sensitivity to aerosols is illustrated by observations showing that the intensity of convective summer storms, and the occurrence of tornado and hailstorms in the eastern United States follow a seven-day cycle determined by week-day pollution (Bell et al. 2009 ; Rosenfeld and Bell 2011 ).

While atmospheric aerosol particles include mineral dust, smoke and marine salts, many biological materials are also involved, e.g., bacteria, archaea, viruses, pollen, spores and organic debris (Després et al. 2012 ; Fröhlich-Nowoisky et al. 2016 ). It was only about a decade ago that researchers noted that the abundance of biological particles in the atmosphere had been “underestimated by atmospheric scientists” (Jaenicke et al. 2007 ). These authors estimated that around one petagram (Pg) or 10 12  kilograms (kg), of such biological particles entered the atmosphere each year—a value comparable to that of mineral dust (~ 2.0 Pg) and marine salt (3.29 Pg) (Jaenicke et al. 2007 ). Particles over forest regions remain poorly characterised in general but assessments indicate that they are diverse and that many (the proportion is unclear) are biological, e.g. potassium rich dust over the Amazon (Poehlker et al. 2012 ). Recent studies, especially those employing methods that can detect and distinguish minute traces of genetic material, have revealed the abundance and diversity of organisms, and organism fragments, in clouds (Fröhlich-Nowoisky et al. 2012 ; Smith et al. 2013 ; Cho and Jang 2014 ; Xu et al. 2017 ). As an example, one study collected three cloud water samples taken from one site in France (Dôme Mountain Meteorological Station) and detected genetic material from more than 28,000 distinct species of bacteria (30 phyla and 286 genera) along with 2600 eukaryotes (from 12 phyla primarily fungi) (Amato et al. 2017 ). Most species appear to be plant epiphytes, pathogens or endosymbionts. A substantial fraction of all these detected organisms appeared to be active and metabolising (producing detectable RNA) (26.4% of the prokaryotes and 82% of the eukaryotes) (Amato et al. 2017 ).

Ice formation

Various cloud properties and behaviours depend on the presence and dynamics of ice crystals (Kanji et al. 2017 ). Ice formation in clouds promotes precipitation. There are multiple processes involved, but one key aspect, named the ‘Wegener-Bergeron-Findeisen process’, is that water vapour accumulates on ice more readily and at lower vapour pressure (lower moisture concentrations), than on water (Storelvmo and Tan 2015 ). Even when the densities of ice are initially low, the effect can multiply as ice crystals collide and fragment within clouds (Mason 1996 ; Phillips et al. 2017 ; Sullivan et al. 2017 ). Outside of the tropics, precipitation is generally associated with such ice forming processes (Mülmenstädt et al. 2015 ; Kanji et al. 2017 ).

Liquid water commonly occurs in clouds at temperatures well below zero (down to –38 °C). Some particles have the ability to induce freezing in liquid water at such sub-zero temperatures. Much remains unknown about such “ice nucleation” particles in the Earth’s atmosphere but particles with biological origins are considered the most abundant and important in many contexts especially at temperatures above − 10 °C (Hoose and Möhler 2012 ).

Ice forming activity occurs in various lifeforms including some bacteria, pollen and fungal spores. Such activity is associated with specific molecules. In some case ice nucleation activity may benefit the organism. For example, the pathogenic rust Puccinia lagenophorae possesses ice nucleation sites on its aeciospores and it has been shown that leaves artificially infected with this fungus and subjected to frost suffer greater penetration of ice crystals into the plants’ tissues, presumably improving access for the fungus (Paul and Ayres 1991 ). But sometimes such activity may be an incidental by-product of other selective processes. For example, cellulose promotes ice formation below –21 °C (Hiranuma et al. 2015 ).

Ice-nucleating organisms are found in rain (Michaud et al. 2014 ; Hara et al. 2016 ; Failor et al. 2017 ). Some are especially effective at promoting freezing, for example, spores of certain rust fungi (specifically, asexual urediospores) capable of long distance atmospheric transport, nucleate ice at temperatures as warm as − 4 degrees centigrade (°C) (Morris et al. 2013 ). We don’t know the degree to which these organisms influence cloud formation or precipitation but the relationships likely operate in both directions. Many particles are washed out of the air by rain, though the impact of droplets on surfaces can also yield increases (Joung et al. 2017 ). Indeed these combined effects are known to modify the composition of airborne bacteria, for example observations in Korea indicate that after rainfall the airborne abundance of some families such as Carnobacteriaceae and Clostridiales typically decreased while the non-spore forming Actinobacteria such as the Propionibacteriaceae increased (Jang et al. 2017 ). Increases in some particles also arise though biological responses. For example, observations near the coast of Southern Norway (Birkenes) indicate that atmospheric concentrations of ice-nucleating particles (active at − 8 °C) increase after rain from May to mid- September but are supressed once snow lies across the landscape. Detection of the sugar alcohols arabitol and mannitol, suggest a fungal source for some of these ice promoting particles (Conen et al. 2017 ). Similar seasonal relationships between ice-nucleating particles and rain have been reported across Eastern Australia (Bigg and Miles 1964 ), the USA (forested areas of Colorado) (Prenni et al. 2013 ), Switzerland (Chaumont) and Russia (Novosibirsk, Siberia) (Conen et al. 2017 ). Laboratory observations have shown that ice nucleating particles are emitted from decaying leaves (Schnell and Vali 1972 ; Schnell and Vali 1973 ) leading to the proposal that the natural abundance of these particles is associated with the fungal activity that results from fallen leaves and sufficient moisture (Conen et al. 2017 ).

Various bacteria (gram positive and negative) possess ice nucleating activity (Failor et al. 2017 ). Certain strains of Pseudomonas syringae (plant pathogens) appear particularly effective, allowing freezing at even comparatively high temperatures (above –10 °C) (Maki et al. 1974 ; Cochet and Widehem 2000 ). Pseudomonas bacteria were proposed as a natural source of atmospheric ice nucleation that might be harnessed to seed rain (Maki et al. 1974 ), before they were detected in natural clouds (Joly et al. 2013 ). Much remains unknown about how such bacteria influence the water-cycle, but we know that their abundances and their ice forming abilities vary among vegetation types, for example being less abundant on conifer trees than most angiosperm species (Lindow et al. 1978 ). Their ice forming abilities likely improve their access to plant tissues (Morris et al. 2014 ). Such mechanisms are restricted to regions where frosts occur and are likely less important in warmer regions. These leaf dwelling prokaryotes may be important determinants of precipitation at mid-latitudes. The ‘bioprecipitation hypothesis’ proposes a cycle in which Pseudomonas and other micro-organisms are lifted off leaves and other surfaces by air currents and promote freezing in clouds, resulting in increased precipitation within the region. This precipitation disperses the microbes and provides the moist conditions both they and their host plants need to grow—thus increasing their prevalence (Morris et al. 2014 ).

Much remains unknown about the behaviour and impact of ice nucleating particles in the atmosphere (Carslaw et al. 2017 ; Coluzza et al. 2017 ) and we know almost nothing about these particles in the tropics (Yakobi-Hancock et al. 2014 ). Methods now permit a much more detailed assessment of bacterial communities and their activities (Hill et al. 2014 ; Failor et al. 2017 ). The bacterial communities on the leaf surfaces of temperate forest trees include widespread generalist taxa, some which vary with time and location, and those that associate with particular tree species (Laforest-Lapointe et al. 2016 ).

• Condensation

Water vapour condenses when air is sufficiently saturated. The threshold depends on temperature, pressure, and available surfaces. All else being equal, condensation occurs at lower vapour concentrations in air containing suitable particles, i.e. condensation nuclei, than otherwise. Thus such particles influence cloud formation and precipitation.

The ability of particles to promote condensation depends on two principle factors: their surface chemistry, i.e. their “hygroscopicity” (the initial layer of water is technically not condensation but adsorption when the water molecules adhere to the particle surface) and their size (particles that are too small tend to evaporate water faster than they can gather it) (Hallquist et al. 2009 ; Després et al. 2012 ). While larger particles, such as pollen and fungal spores may be able to promote droplet formation without further size increases (Pope 2010 ; Hassett et al. 2015 ), smaller particles must grow before they can play this role.

The surface chemistry and size of atmospheric particles can both be modified by the products that result from the breakdown of various volatile organic compounds (VOCs) in the atmosphere. About three quarters of these VOCs are relatively reactive and last less than one day in the atmosphere, with most, including isoprene and pinene, surviving just a few hours (Guenther et al. 1995 ). Various chemical pathways are involved though few are well studied. For example, we know that hydroxyl radicals play a key role in the rapid modification of isoprene over tropical forests, and that these radicals appear to be regenerated rather than depleted during this process (Taraborrelli et al. 2012 ). In general, chemical changes mean that most of these organic compounds lose their volatility due to reactions with other molecules, sunlight and radiation (e.g., Cappa 2016 ). Some may aggregate and precipitate directly. Most will adhere to surfaces (Ehn et al. 2014 ). These sticky compounds can accumulate allowing even the smallest particles to grow, and to reach sizes where they can promote droplet formation.

Most VOCs have biological origins and forests are major sources (here I follow convention and exclude methane though this is the most abundant organic gas (Bousquet et al. 2006 ; Kirschke et al. 2013 ; Tian et al. 2016 )). The atmosphere receives over one Pg (10 12  kg) of biological carbon as biogenic VOCs (“BVOCs”) annually (Guenther et al. 1995 ). The carbon associated with these emissions are approximately 1 % of the 120–130 Pg of carbon each year (C∙yr. − 1 ) of terrestrial gross primary production (see for example, Parazoo et al. 2014 ). The main constituent appears to be isoprene (~ 44%) with most of the rest comprised of various monoterpenes such as pinene (~ 11%) and other oxygenated carbon compounds (Guenther et al. 1995 ). Isoprene is produced primarily when plants are stressed by heat, with global emissions estimated at 0.44 to 0.66 Pg C∙yr. − 1 concentrated over the tropics (Guenther et al. 2006 ), while pinene is locally abundant over temperate conifer forests in summer (Guenther et al. 1995 ).

Isoprene emissions vary among plant species. While many tree species are significant sources, this is not the case for grasses. Thus isoprene concentrations are typically higher over forests than grasslands. Indeed major emissions, with considerable local variation have been reported over the Amazon (Gu et al. 2017 ). The ability of isoprene to increase cloud cover during periods of heat-stress, thus lowering temperatures and perhaps stimulating rain remains to be investigated (Sheil 2014 ).

Modern methods reveal hundreds of naturally occurring BVOCs each with their own distribution, chemical dynamics, and impacts. Many result from plants, some a result of stress or damage or of phenological state, with each species having its own range of compounds (Laothawornkitkul et al. 2009 ; Lerdau and Slobodkin 2002 ; Holopainen and Blande 2013 ). Indeed the production of many BVOCs appears species (even genotype) and condition specific (Llusia et al. 2002 ; Yuan et al. 2009 ). One study found that a seedling of Scots pine ( Pinus sylvestris ) emits at least 20 distinct monoterpenes (Heijari et al. 2011 ) and just one of these, limonene, can become over one thousand distinct compounds in the atmosphere (Kundu et al. 2012 ; Holopainen and Blande 2013 ). Our ability to detect and distinguish these compounds is improving: for example, one study over just one citrus orchard in the USA detected and tracked the varying atmospheric abundance of over 500 different organic compounds derived from the vegetation (Park et al. 2013 ).

Trees and forests are not the only source of natural biological aerosols. Marine organism emit various BVOCs into the atmosphere including isoprene and monoterpenes (Shaw et al. 2010 ). Particular attention has been given to dimethyl sulphide, a compound emitted by various phytoplankton and reef building corals particularly when they are stressed (Stefels et al. 2007 ; Fischer and Jones 2012 ; Jones 2013 ). This volatile compound oxidises to generate sulphuric acid in the atmosphere and has long been suggested to play a role in promoting condensation and cloud formation (Stefels et al. 2007 ; Ayers and Cainey 2008 ). We remain uncertain how influential these processes are but the runoff, sediments and smoke that often results from deforestation and other land cover related processes can impact marine life, suggesting that emissions associated with these organisms would be affected (Abram et al. 2003 ; Prouty et al. 2014 ; Ramos-Scharrón et al. 2015 ; Teneva et al. 2016 ).

Anthropogenic impacts

Though specific information is limited it is generally assumed that atmospheric aerosol concentrations were lower in the pre-industrial era (reviewed in Hamilton 2015 ; Carslaw et al. 2017 ). In such conditions the climate system is thought to have been more sensitive to changes in these concentrations (Spracklen and Rap 2013 ; Carslaw et al. 2017 ). Over the past century the products of industry, fires and other activities have added considerably to atmospheric particles though many details of these emissions and their dynamics remain unclear (Fuzzi et al. 2015 ; Sánchez Gácita et al. 2017 ). At the same time changes in land cover and climate have modified BVOC emissions (e.g., Hewitt et al. 2009 ; Yue et al. 2015 ).

Studies indicate that human activities impact on the abundance and activity of biological ice-nucleating particles in the atmosphere. For example, observations in France indicate that atmospheric acidification reduces their influence (Pouzet et al. 2017 ). Nonetheless evidence that human activities have impacted ice nucleating particles or their properties remains too limited to generalise (Carslaw et al. 2017 ; Coluzza et al. 2017 ).

More generally, there has been some effort to identify how changes in land cover, and other human activities, impact aerosols and their influence on climate. Much of this work has focused on smoke and industrial pollution rather than on natural aerosols. One synthesis concluded that land use change through the twentieth century likely led to cooling with between 10 and 50% of this effect due to anthropogenic aerosol emissions (they did not consider precipitation directly) (Heald and Spracklen 2015 ). These authors acknowledged many unknowns including the interactions that occur among these processes (Heald and Spracklen 2015 ). Where processes have been jointly considered they sometimes have conflicting implications. For example, pollution may mask some of the influences of forest loss on Amazonian rainfall (Cox et al. 2008 ). Interactions can also be complex, for example, the isoprene derived particles found over the Amazon typically adhere to each other allowing aggregation and increased size but smoke reduces this aggregation (Bateman et al. 2017 ). As another example, while forest loss generally reduces BVOC emissions, some land uses are major sources. For example, one study found that oil palm plantations in Malaysia emitted about seven times more isoprene per unit area than the forest they replaced (Hewitt et al. 2009 ). The implications of all these processes for the global water cycle remain largely unexplored.

Winds and atmospheric circulation

A role for temperature.

A predictive understanding of atmospheric water transport must include atmospheric circulation, winds, and the factors that determine them. Edmund Halley, a contemporary of Isaac Newton and still widely known for predicting the periodicity of a comet, first suggested that global atmospheric circulation was determined by temperature gradients (Halley 1686 ). Halley’s ideas were intuitively appealing as they fitted with the recognised phenomena of sea-to-land winds or sea breezes which arise when the land is warmer than the ocean (Miller et al. 2003 ) (Fig.  1 ). They also explained monsoon cycles as a result of the seasonal switch as land-ocean temperatures gradients switch direction from warmer-ocean to warmer-land and back. These seasonal shifts in wind direction impact moisture transport and precipitation.

A schematic of a temperature drive sea breeze. Air rises over the warmer land surface, lowering local air pressure and drawing in moisture laden air from over the ocean. This air converges, rises and cools, allowing the moisture it carries to condense and fall as precipitation

Halley’s temperature-gradient theory , with added details (Hadley 1735 etc.), remains the dominant explanation of how winds and global circulation patterns are generated (Schneider et al. 2014 ; An et al. 2015 ). The details include circulation cells and their seasonal shifts, and the influence of Earth’s rotation. Conservation of angular momentum, an effect known as the Coriolis Effect, deflects winds in the northern hemisphere rightwards and those in the southern hemisphere leftwards. Nonetheless, the force and energy that drives winds and circulations derive from differences in temperature. The modern perspective highlights how global circulation patterns migrate as sunlight and temperature gradients shift with the monsoon region lying between the annual extremes reached by the intertropical convergence zone (Li and Zeng 2002 ).

Various research interpreted from within the temperature-gradient theory implies a role for forest beyond passive moisture recycling (e.g., Boers et al. 2017 ; Wright et al. 2017 ). For example, one study was interpreted as showing that transpiration from the forest provided the primary moisture source for rainfall during the transition that facilitates the seasonal (monsoon like) transition from dry to wet conditions in the southern Amazon (Wright et al. 2017 ). Models have been used to investigate many details in these relationships, and their dependencies, but all these simulations assume that the temperature-gradient mechanism is correct and adequate.

No-one questions that temperature gradients can generate sea breezes, seasonal shifts in weather and convective weather systems. A more debated question is whether these processes are sufficient to explain atmospheric motion and moisture transport. Researchers recognise challenges in applying the temperature-gradient theory  to global circulation. For example, the ascent of warm air drives the process, but as this air rises, other air must descend (the system circulates). But as air descends it warms and thus gains buoyancy resisting this circulation. Estimates of heat loss imply that this resistance should prevent circulation (Goody 2003 ). What then are the alternatives?

A role for water vapour

Anastassia Makarieva, Victor Gorshkov and various colleagues—recently including myself—have advanced a theory describing how evaporation and condensation influence atmospheric dynamics. This is the first theory indicating that condensation plays a general and dominant role in atmospheric dynamics (though others have suggested a role in cyclonic storms, see Lackmann and Yablonsky 2004 ; Wacker et al. 2006 ).

The conventional temperature-gradient theory assumes that all the dominant processes that determine atmospheric pressure gradients can be understood without considering the changes in molecular (particle) densities that occur as water evaporates and condenses. The new mechanisms arise when we seek a more complete picture. I will briefly sketch some of the key principles. Those seeking more detail should refer to Makarieva and Gorshkov ( 2010 ), Makarieva and Gorshkov ( 2007 ) and Makarieva et al. ( 2013 ).

Water vapour is unevenly distributed in the atmosphere—imbalances are maintained by the constant interplay of evaporation and condensation. In all but the driest regions of our planet the concentration of water vapour declines markedly with altitude over the first kilometres in the lower atmosphere. It takes energy to evaporate water: i.e., to free the molecules from each other as well as work against local atmospheric pressure to create space for the additional gas. Thus atmospheric water vapour stores energy.

When condensation occurs in the atmosphere stored energy is released—some is converted to heat (either radiated away or warming the local atmosphere), some (the gravitational energy) is dissipated to friction via the acceleration and motion of the falling water (n.b. some of this gravitational energy is tapped in hydroelectric schemes), and the remainder can accelerate air as it generates a pressure gradient (for a discussion of the relative values in the context of global circulation see, Makarieva et al. 2013 ). It is this final process, the ability of condensation to accelerate air, which was previously overlooked (Makarieva et al. 2013 ; Makarieva et al. 2017 ).

How does this acceleration occur? If we compare an atmospheric column over a moist humid region with one over a drier region we will find that the relationship of air pressure (and temperature) with altitude differ. If these columns are placed beside each other we find that the moist column maintains lower pressure at low altitude and higher pressure at high altitude than the drier column. This difference in pressure with altitude generates circulation such that the moist column (where most condensation is occurring) will draw in low-level air from the drier region, and return air to it at a higher-level. This moist column now rises and cools and the resulting condensation leads to a drop in atmospheric pressure at the lowest altitudes drawing in yet more moist air which rises, cools and condenses in turn. This process can be sustained as long as there is sufficient water vapour to fuel the process. The resulting pressure gradients, and expected rates of energy generation (power) associated with these processes are comparable to observations (Makarieva et al. 2013 ).

Rates of evaporation and condensation are controlled by different factors. Condensation dominates the spatial patterns resulting from these processes because, while evaporation is a slow and widely distributed, energy-limited process, increasing local pressure gradually over large areas, condensation can be both rapid and localised. Powerful storms arise when large volumes of moist air rise rapidly in a constrained region leading to intense condensation (Makarieva et al. 2013 ). This idea predicts that storm power is linearly related to total rate of precipitation—this prediction matches observations (Makarieva et al. 2015 ; Sabuwala et al. 2015 ).

Fuller details of the theory and its implication can be found in physics journals (Makarieva and Gorshkov 2009 ; Gorshkov et al. 2012 ; Makarieva et al. 2014 ) and in the atmospheric and meteorological science journals (Makarieva et al. 2013 ; Makarieva et al. 2013 ; Makarieva et al. 2017 ; Makarieva et al. 2017 ). We also summarised the ideas for non-specialists (Makarieva and Gorshkov 2010 ; Sheil and Murdiyarso 2009 ). Furthermore, we have described failings in the temperature-driven theory of winds (Makarieva et al. 2015 ) and revised the fundamental equations governing atmospheric dynamics (Makarieva et al. 2017 ). As I shall summarise in the following section we also examined the influence of forests.

The breeze from the trees

A key implication of the condensation-driven theory of winds is that regions that generate high evaporation rates relative to surrounding regions develop lower-pressure zones which draw in air. This air converges, rises and cools and moisture condenses, generating rainfall that can surpass local evaporation. All else being equal, the difference in mean evaporation between adjacent regions predicts the wind between them. Regions with higher leaf area are thus expected to attract winds from areas with lower leaf area (Makarieva et al. 2013 ). This relationship implies that sufficiently large areas of tree cover actively draw in air and moisture from elsewhere. This process is called the ‘biotic pump’.

The attraction of transpiring vegetation for moist air has been recognised previously. For example, there is evidence from dryland southern Africa that the delayed increase in leaf area that follows rainfall reinforces subsequent winds and precipitation such that `the vegetation draws airflow toward itself in a self-sustaining way` (Chikoore and Jury 2010 ). Similar observations concern monsoon systems (see below).

The biotic pump explains various phenomena. It explains how high rainfall is maintained in the continental interiors of the Amazon, Congo and Siberia, while in areas without forest the declines in rainfall with distance inland is steeper (typically halving each few hundred kilometres over level terrain in an approximately exponential decline) (Makarieva and Gorshkov 2007 ; Makarieva et al. 2009 ; Sheil and Murdiyarso 2009 ; Makarieva et al. 2013 ). Neither global circulation patterns nor regional recycling can explain these patterns—they could influence the rate of decline with distance but not negate it. This effect—the drawing of rain into continental interiors—requires a biologically functioning forest, so we would predict that the effect will be smaller over boreal forests in deep winter (when transpiration ceases). Observations support these predictions (Makarieva et al. 2013 ; Sheil 2014 ). The low pressure generated over forests can explain how the wind called the “Caribbean Low Level Jet” opposes the prevailing trade winds as it is drawn towards the South American continent (Poveda et al. 2014 ). There is considerable scope for further evaluating these relationships.

Instabilities and implications

Among the insights provided by recognition of positive feedbacks in land-cover climate change relationships, is the potential to switch depending on how evaporation differs among neighbouring regions. These switches can occur on a regular basis as in monsoons or more permanently. Though the idea of alternate ecologically determined states is established (Scheffer et al. 2001 ), such climate switching remain poorly characterised. Such behaviours warrant evaluation.

As noted previously, temperature based models do not match the observed switching behaviour of monsoons (e.g., Acharya et al. 2011 ; Niu et al. 2015 ). Additional controversy surrounds mechanisms and the causes of annual variation (Boos and Storelvmo 2016 ; Levermann et al. 2016 ). Furthermore, the abrupt shifts in monsoon climates sometimes seen in paleo-data remain unexplained (Herzschuh et al. 2014 ). The temperature driven theory suggests we should find a clear difference in land-ocean temperature contrasts between seasons and as an explanation of when switching occurs—in practice such a pattern is absent. Indeed, Antonio Nobre (pers. comm., see also, Nobre 2007 ) talks about the “Cold Amazon Paradox” as the strange state of affairs when the strongest winds blow from the Atlantic into the Amazon not as expected—from a naïve temperature-gradient theory derived perspective—when the Amazon is warmest, or the temperature contrast greatest, but when the Amazon is markedly colder than the ocean (see Fig.  2 , for a fuller examination of regional moisture flows in this region see Drumond et al. 2014 ).

The Cold Amazon Paradox: during the wettest months the land is colder, not warmer, than the ocean. We compare two areas (top panel) land in the Amazon, green-lines (all land between 70 W and 40 W, 2.5 N and 7.5S), and ocean, blue-lines (sea at 40 W-20 W, 2.5 N and 7.5S). Upper graphs: Monthly rainfall and surface temperature o C (at 1000 hPa). Lower graphs: winds: meridional (south to north) and zonal (west to east). These mean values were derived from 1978 to 2013 using data from the National Centers for Environmental Prediction–National Center for Atmospheric Research (NCEP–NCAR) reanalysis (Kalnay et al. 1996 )

The biotic pump offers an alternative explanation. The switch between dry and wet conditions found in monsoon climates arises from the positive feedbacks that occur as the predominant difference in evaporation rates kick the prevailing winds from a land-to-sea to a sea-to-land configuration (Makarieva and Gorshkov 2007 ; Sheil and Murdiyarso 2009 ; Makarieva et al. 2013 ). The most extreme seasonal switch occurs in the boreal forests where transpiration and thus inland moisture transport is predicted and observed only when transpiration can occur (Makarieva et al. 2013 ; Sheil 2014 ).

Observations in the tropics show that evergreen forests maintain relatively high humidity year round including dry periods (Bunyard 2014 ). The evergreen forests of the seasonal Amazon also maintain significant transpiration through the year (Myneni et al. 2007 ; Wu et al. 2016 ). Recent studies indicate that the ability of the Amazonian forests to maintain transpiration in the dry season plays a key role in determining the dry-to-wet season transition in the southern Amazon (Wright et al. 2017 ). The “dry-season” transpiration typically permits some rainfall and this retained moisture facilitates the return of the wet season. The region’s more balanced land-sea evaporation contrast also explains the absence of the abrupt switching of onshore winds found in drier monsoon regions (Zhou and Lau 1998 ). Overall, it appears that the switching behaviour suggested by the biotic pump appears to match observations, though other explanations have also been proposed (e.g., that 'shallow convection' maintains moisture locally (Wright et al. 2017 )).

The diurnal weather cycle over forest can also be seen as a daily monsoon. I will use this example to illustrate and evaluate the role of evaporation and condensation (for more information see Makarieva et al. 2014 ). To explain our predictions, first consider an idealised case (see Fig.  3 ). Note that, all else being equal, precipitation is more likely in a wetter atmosphere (Holloway and Neelin 2010 ). Note too that any local increase in gas molecules, water vapour included, will raise local atmospheric pressure. Thus if we compare days with and without rain, in an area generating rain we predict that on rainy days we will observe greater local atmospheric pressure just prior to rain falling, i.e. more water vapour raises both atmospheric pressure and the likelihood of subsequent rain. To evaluate this prediction, we gathered data for pressure and precipitation from 42 meteorological stations divided over three regions (one within and two outside the Amazon forest). These data were provided by the Brazilian Meteorological Institute. We used all the available data for each station up to the end of 2012 (the longest running provided 53 years of data, see www.inmet.gov.br/portal/index.php?r5bdmep/bdmep ). To summarise the results: rainy days within the forested Amazon region are, consistent with the accumulation of more water vapour, preceded by a period of higher atmospheric pressure greater than any such pattern on rainless days (detected at 13 of 14 stations). In the peripheral and more deforested regions the results are less consistent with most sites showing some drop in pressure prior to rain (around two thirds of the stations indicate decreased pressure). We believe that these latter sites do not generally sustain enough evaporation to trigger rain locally but that air movements are initiated elsewhere (Makarieva et al. 2014 ). While these patterns are not easily explained by temperature effects alone, they conform to the predictions of the biotic pump. The effects of temperature and moisture dynamics on winds clearly require further study (Makarieva et al. 2015 ).

A schematic of how condensation driven winds develop between ocean and forest. a Morning: the atmosphere is still and dry (pink colour). Once the sun rises the forest emits water vapour (vertical arrows) at a greater rate per unit area than the ocean. Slowly, through the day ( b ) and ( c ) moisture accumulates over the forest (bluer colour), until ( d ) the water vapour over the forest is sufficient to condense (possibly accelerated by aerosols). This condensation reduces local air pressure thus drawing in moist air from elsewhere (horizontal arrows). In contrast to the slow evaporation of water vapour, condensation occurs quickly, and leads to air being drawn in, converging, rising, cooling and condensing additional moisture in a self-sustaining process. Moisture generated locally via forest evaporation precipitates together with much additional moisture brought from the ocean. This additional moisture is what ensures land remains wet counteracting the loss of water via rivers to the ocean

The diurnal and annual monsoon cycles show how changes in evaporation and condensation can potentially switch a region from wet to dry. Such switching can also occur at longer timeframes (Makarieva and Gorshkov 2007 ; Sheil and Murdiyarso 2009 ). If inland rainfall depends on large near-contiguous forest, then deforestation, especially near the coast, risks switching the continent from wet to dry—with catastrophic implications. The precursor of such a switch would be declining rainfall and reduced reliability. This fits with patterns of declining rainfall in southwest Australia (averaging a 21% reduction relative to coastal values) being due to the reduction of native woody cover from 60% to 30% between 1950 and 1970 (Andrich and Imberger 2013 ). It also fits with declining reliability in rainfall as correlated with forest loss on the Atlantic coast of Brazil (Webb et al. 2005 ). The increasing desiccation, and more frequent droughts, can result in tree death, increased flammability, fires, and further drought (Zemp et al. 2017b ).

Alternative explanations require examination too. Some also identify positive feedbacks and the possibility of switching states (e.g., Boers et al. 2017 ; Wright et al. 2017 ). Others suggest that more gradual transitions are possible (Levine et al. 2016 ; Zemp et al. 2017a ). It is crucial to distinguish which theory or theories best conform to reality and the risk of climate switching. Observing how air pressure, vegetation behaviour, and precipitation vary over the diurnal and monsoon cycle can provide key insights.

If regional patterns in the relative abundance of water vapour generate and stabilise winds, then both reduced tree cover and increased atmospheric carbon dioxide (inducing reduced stomatal opening, which leads to lower water-use, see e.g., de Boer et al. 2011 ) will reduce atmospheric moisture, leading to reduced continental precipitation and related winds. Long-term data already indicate a long-term decline in wind intensity over the tropics and mid-latitudes (McVicar et al. 2012 ) not all of which can be ascribed to changing surface roughness (Wever 2012 ). Shifts in circulation cell boundaries are also predicted with major impacts for the areas affected (Heffernan 2016 ; Makarieva et al. 2017 ). The eastward shift of the rainfall zone over South East Asia may be such an impact, perhaps arising from interactions between regional circulation patterns and forest loss (Tokinaga et al. 2012 ; Sheil 2014 ).

If condensation can indeed determine wind patterns, then aerosols that promote condensation, or freezing, may influence regional climate to a greater degree than already recognised. The biotic pump implies that the locations where condensation starts most readily and frequently are those that draw in winds. All else being equal, this will be over the areas that evaporate the most moisture. But aerosols can change this by permitting condensation at lower vapour concentration and shifting the balance. This offers an alternative means by which vegetation can influence precipitation and winds.

Our work on cyclonic systems—hurricanes, typhoons and cyclones—suggests that forests may reduce the frequency and intensity of storms, especially those that develop near land. Given their high vapour emission it may initially seem that forests should generate and support cyclonic storms. This does not occur because, unlike oceans, forests possess a marked diurnal cycle with reduced transpiration overnight, moreover drag-friction over forests is severe, absorbing energy and slowing winds. Furthermore, while cyclonic storms concentrate air flows and resulting condensation into their eye, forests release moisture and aerosols in a more diffuse form, ensuring that condensation remains more broadly spread in both space and time. Thus cyclonic storms cannot form or be sustained over, or near to, extensive forests. In addition, given the need for water vapour to fuel these storms, if forests constantly draw moisture away as the biotic-pump theory suggests then they would reduce the energy available to fuel storms in nearby oceans. The combined result of all these process means that storms are unlikely to form near to extensive areas of forests, and any storms carried by the prevailing winds towards such forests are likely to decline in power.

Cyclones generally form over the ocean at latitudes where large amounts of water vapour are available, that is within two belts 10°–20° north and south of the equator: latitudes that lie between those of wet tropical forests and dry deserts (deserts yield only dry air), where the desiccating effect of neither dominates. The inhibiting effects of forests to either side likely explains why cyclonic storms are rare in the South Atlantic (Hurricane Catarina in 2004 was the only exception). Loss of the Amazon and Congo forests would increase the likelihood of such storms. Any such protective properties are scale-dependent, and while the influence of large forests such as those in the Amazon are likely extensive, the impacts of small areas will also be small. For example, few Caribbean islands possess sufficient areas of forest to greatly influence cyclonic storms—though such properties could be boosted by large-scale rehabilitation.

A jigsaw with missing pieces

We know enough to recognise that our picture of how the global climate system works is very different than how it was viewed even a few years ago. We also know enough to recognise that much remains unclear. Here I will briefly note a few intriguing topics for research (see also Sheil and Murdiyarso 2009 ) before considering some practical aspects.

New insights

Insights into vegetation-atmosphere relationships can advance, and draw upon, many disciplines. For example, there are fundamental biological questions such as why plants use as much water as they do (Cramer et al. 2009 ; Wolf et al. 2016 ). We also need to understand how plant traits that influence wider water availability evolve in response to natural selection.

Research can improve understanding of the processes and relationships that underlie the biotic pump. While laboratory evaluations appear theoretically feasible, see for example the ideas in appendix 4 of Makarieva et al. ( 2013 ), in practice it is technically demanding to separate the effects of temperature, buoyancy and molecular densities in an enclosed apparatus (e.g., Bunyard 2014 ; Bunyard et al. 2017 ). Furthermore, small-scale studies may remain difficult to interpret in the context of real large-scale atmospheric behaviours. Unambiguous tests may require field observations. I encourage creative researchers to explore these problems.

There is plenty to examine in current meteorology too. For example, the daily precipitation patterns that are characteristic in many regions of the tropics remain poorly understood (Kikuchi and Wang 2008 ; Sakazaki et al. 2017 ). Recognition of biological processes may help (Makarieva and Gorshkov 2007 ; Sheil and Murdiyarso 2009 ; Sakazaki et al. 2017 ;). We know that transpiration often ceases temporarily, or periodically, after high rates have been achieved (Zhang et al. 2013 ). This may disturb local pressure dynamics and thus influence cloud dynamics and precipitation. The pulsing patterns of moisture release, and resulting raised humidity, indicated over at least some forests (see Bunyard 2014 ) may be one way for the forest to generate the vapour concentrations required to trigger condensation—though the mechanisms underlying this behaviour and how it might have evolved remain unknown.

There are longer cycles to be explored too, for example, rainfall correlates to lunar phases (Brier and Bradley 1964 ; Carpenter et al. 1972 ; Pennycuick and Norton-Griffiths 1976 ; Cevolani et al. 1987 ; Hanson et al. 1987 ; Roy 2006 ) and again physical explanations have been elusive (Camuffo 2001 ; Kohyama and Wallace 2016 ). But such rhythms may be biological in origin (for examples see, Reinberg et al. 2016 ; Zajączkowska and Barlow 2017 ). Indeed, some older studies noticed how, for example, the presence of ice nucleating particles also varied with the lunar cycle (Bigg 1963 ; Bigg and Miles 1964 ).

At longer time-scales, our understanding of past events may require reassessment too. For example, concerning the role of humans and fire use in the formation, expansion and maintenance of drylands often ascribed to climate alone. The desiccation of Australia may be an example (Makarieva and Gorshkov 2007 ; Sheil and Murdiyarso 2009 ). Another possible example is the savanna vegetation that reaches the west African coast between Ghana and Nigeria (Savenije 1995 ; Salzmann and Hoelzmann 2005 ). We should also consider the climatic influence of people in paleo-extinctions where past analysis consider human activities and climate change as distinct (Cooper et al. 2015 ; Stuart 2015 ). Similarly it may raise new factors regarding the causes and role of declining rainfall in the history of various civilizations, from the Maya of Central America, to the Axumites of Eastern Africa and the Polynesians of Easter Island (Douglas et al. 2016 ; Rull et al. 2016 ; French et al. 2017 ).

Advances in theory, methods and data handling provide new opportunities. For example, genetic methods now permit the detection and identification of very low concentrations of airborne microbes (Hill et al. 2014 ; Failor et al. 2017 ). At a larger scale, while challenges remain (Maggioni et al. 2016 ), satellites and models already permit the monitoring of global patterns in precipitation and wind patterns (Spracklen et al. 2012 ). There are major research efforts looking at aerosol particles and their origins, dynamics and influences and new discoveries remain frequent (Failor et al. 2017 ; Gu et al. 2017 ). I expect surprises.

Water security and the imperative of improved understanding

The lives and livelihoods of billions of people depend on reliable access to water (Sheil 2014 ). We must safeguard the processes that this access depends on. For that we need to understand how the hydrological cycle works and what it depends on. Despite recent progress, this knowledge remains fragmented and incomplete. One consequence is that models and their predictions remain unreliable (Trenberth 2011 ; Stevens and Bony 2013 ; Shepherd 2014 ; Marotzke et al. 2017 ).

So what do we know? We know that the hydrological cycle is changing and that this is impacting people and the environment (Stocker et al. 2013 ; Hegerl et al. 2015 ; Mekonnen and Hoekstra 2016 ). We know that changes in land cover impact atmospheric moisture (Sterling et al. 2013 ), air temperature (Alkama and Cescatti 2016 ), aerosols (Heald and Spracklen 2015 ) and air movements (Detto et al. 2008 ; Santana et al. 2017 ). We know that the hydrological cycle is influenced by multiple feedbacks at multiple spatial and temporal scales (Mahmood et al. 2013 ; Wang-Erlandsson et al., 2017 ) and that trees and forests play a significant role (Bonan 2008 ; Spracklen et al. 2012 ; Morris et al. 2014 ; Sheil 2014 ; Ellison et al. 2017 ; Wei et al. 2017 ).

We know what aspects matter even if we don’t yet know or agree the details. For example, we know that the flow of water vapour from the land surface depends on many factors, not all of which are fully characterised or represented in models (and the many simulations, such as the IPCC scenarios, that depend on these). Such effects may oppose each other, making the outcome unclear, for example, we know that forest loss and reduced stomatal opening associated with increasing carbon dioxide is likely to reduce vapour transpired to the atmosphere (Spracklen et al. 2012 ; Sheil 2014 ; Franks et al. 2017 ), but increasing leaf area observed in many regions may also boost transpiration (Zhang et al. 2015 ).

Complexity means that some relationships, such as the effects of aerosols, may defy easy generalisation. But others, notably fuller inclusion of evaporation and condensation processes in atmospheric dynamics (the ‘biotic pump’), offer elegant insights and, if integrated into more comprehensive models, may resolve some of the discrepancies plaguing current climate models.

While evidence shows that climate is influenced by tree cover (locally and elsewhere), not all tree cover has equal effects. Some properties reflect the species and genotypes present (volatile gas emissions, leaf phenology). While a large area of planted forest will certainly influence the local water-cycle, it is not yet clear how when and where this can replace the various properties and functions of natural forest. For example, we know that to a greater degree than most planted forests, many natural forests maintain low understorey temperatures during the day and generate a local atmospheric inversion at night maintaining a moist understorey that will influence how and when water vapour is released (Szarzynski and Anhuf 2001 ). Tree diversity may stabilise climate feedbacks by reducing vulnerability to changing conditions and to disturbance (e.g., Schurr et al. 2006 ; Hisano et al. 2017 ; O’Brien et al. 2017 ). In any case, younger vegetation has distinct properties when compared to more mature vegetation and we must acknowledge that the impacts of restoration and forest recovery are dynamic (Bruijnzeel 2004 ; Filoso et al. 2017 ). Hydrological impacts are context dependent: a site can only influence water that is available (in the vicinity). So, for example, while there was optimism that increasing tree cover in the arid regions of northern China would increase rainfall and initiate wider greening even without explicit attention to long-range water transport (e.g., Jiang and Liang 2013 ), recent appraisals suggest little progress in the driest areas (Ahrends et al. 2017 ). Some studies suggest that planting (Deng et al. 2016 ) and alien species (Cavaleri et al. 2014 ) can be more disruptive and less beneficial than natural recovery by native vegetation. Nonetheless, such differences require more study before broad generalisations are justified as there may be exceptions or management options that can reduce or negate such differences (Sheil and Murdiyarso 2009 ).

Sustaining a resilient and reliable water cycle is a global challenge, and requires understanding and action at many levels. While I have emphasised biophysical relationships, the challenges and opportunities cannot be addressed by the biophysical sciences alone. As links and dependencies are identified at local, regional and trans-continental scales there will be a major role for those concerned with devising and implementing the social and institutional arrangements required (see for example, Cohen 2012 ; Ellison et al. 2017 ; Keys et al. 2017 ).

Among the most profound and disturbing insights offered by this review is the potential for non-linear behaviours: the indication that a continent or region that passes some threshold of forest loss might tip from a wet to a dry climate. While various details remain poorly characterised, and some are debated, the overall linkages appear uncontroversial. We know that large scale forest loss or die-back will generally reduce atmospheric moisture, rainfall and cloud cover, and increase the likelihood of drought and further loss or die-back. Add in human activities, increasing temperatures and fires, and changes could be rapid, making whole regions near uninhabitable and releasing vast amounts of carbon stored in vegetation and soils into the atmosphere over only a few years. There is also a positive side: rainfall can be stabilised and regained by maintaining and restoring tree cover. Characterising these threats and opportunities is a priority.

Life depends on water while water frequently depends on life. Understanding these dependencies is crucial in ensuring the reliable availability of fresh water. We know that forests and trees play a major role though many details remain debated. In the future, forests should be protected, managed and planted, at least in part, for their role in sustaining atmospheric water and all that depends on it. Much now depends on improving our understanding. Forest scientists and other biologists have a major role to play.

Note that like precipitation, evaporation is represented in units of depth, e.g., the equivalent depth of water. This also clear from considering the water involved as a volume (length cubed) divided by an area (length squared) giving units of depth (length).

Abbreviations

Biogenic VOCs

The Intergovernmental Panel on Climate Change

Degrees Centigrade

Petagram or 10 12  kg

Volatile organic compounds—molecules that can occur as gases in the atmosphere and whose chemical structure includes carbon (but excluding carbon dioxide, carbon monoxide, all carbides, and carbonates). While methane is formally a VOC it is often excluded

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Acknowledgements

Many ideas presented here are the result of discussions with colleagues, particularly Anastassia Makarieva and Victor Gorshkov who also provided detailed feedback on earlier drafts. I am grateful for the insights and suggestions of two anonymous reviewers as well as to Jan Vermaat, Rannveig Margrete Jacobsen, Antonio Donato Nobre and Peter Bunyard for comments on a near final draft. I thank Miriam van Heist for help with document review and preparation.

DS’s time was paid by the Norwegian University of Life Sciences. He acknowledges the value of participation in the Australian Research Council projects under grants DP160102107 and LP130100498. DS also benefitted from the meeting in Leuven, Belgium in 2015 where his participation was funded by WeForest and the Center for International Forest Research, and also from the meeting in Wageningen, Netherlands, also in 2015, where his participation was funded by Tropenbos.

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Sheil, D. Forests, atmospheric water and an uncertain future: the new biology of the global water cycle. For. Ecosyst. 5 , 19 (2018). https://doi.org/10.1186/s40663-018-0138-y

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